Tectonic Boundary Objects in Europe
Named tectonic boundary objects as they appear on the HIKE European fault database. The determing factors for the hierarchical ranking of the tectonic boundaries are primarily their present-day spatial relation and secondly their kinematic linkage during at least deformation phase. All named tectonic boundary objects are identified by an ID representing a two-letter country-specific prefix. Fault systems and/or fault domains crossing political borders are shared by several countries. Therefore, they can contain faults from different countries, indicated by the country-specific prefixes to the respective ID.
Tectonic Boundary in Belgium
All named tectonic boundary objects that are located (at least partly) in Belgium, are identified by an ID with the prefix „BE“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Belgium, displayed in the HIKE European fault database.
Jupille Fault
Aguesses-Asse Fault
There is still ongoing discussion about the connection between the two faults. Either they are two individual faults or they form a continuation of each other, separated by a sinistral transverse fault. Furthermore there is a discussion of the importance of the Aguesses-Asse Fault. Either it is a minor thrust separating the Herve and Liège units, both located north of the Variscan front thrust or it is a major thrust constituting an eastern segment of the Variscan front thrust and continuation of the Eifelian Fault (Cambier G. & Dejonghe L., 2010).
The Aguesses and Asse Faults are both thrust faults of Variscan age (Cambier G. & Dejonghe L., 2010).
Aguesse Fault
Asse Fault
José Fault
Borzée Fault
Ardenne basal detachment
Ardenne thrust
Haine-Sambre-Meuse fault system
System of major Varsican thrust faults in Belgium with an east-west direction. The system is located directly north of the Midi fault (Delmer A., 2000; Belanger I. et al., 2012).
Masse Fault
Malonne Fault
Saint-Pierre Fault
Ormont Fault
Tombe Fault
The Tombe Fault was first described by Smeysters (1880). The fault dips gently to the south and is connected to other fractures related to the Midi Fault (Cambier G. & Dejonghe L., 2012).
Chamborgneau Fault
Aachen Fault
Discussion is ongoing about the connectivity of the Midi-Eifelian Fault and the Aachen Fault. Either the Aguesse-Asse Fault or the Tunnel Fault connects these two major Variscan thrust faults (Cambier G. & Dejonghe L., 2012).
The Aachen fault is a thrust fault of Variscan age and is the continuation of the Variscan thrust front in the east of Belgium towards Germany, where it is crosscut by the Feldbiss Fault Zone of the Roer Valley Graben (Cambier G. & Dejonghe L., 2012).
Eupen Fault
The out-of-sequence Eupen Fault is thought to crosscut, merge with and postdate the Theux Fault in the southern part of the Theux Window. Therefore the Eupen Fault forms the south/southwestern boundary of the Theux Window (Cambier G. & Dejonghe L., 2010).
The Eupen Fault is a thrust fault of Variscan age. It branches off the Theux–Tunnel Fault and locally forms the southern boundary between the Vesdre Nappe and the Stavelot Massif (Hance et al., 1999).
Midi Fault
The Eifel and Tunnel Faults are assumed to be the eastern continuation of the Midi Fault, yet there is still a lot of uncertainty in this area (see ScopeNote of Aguesses-Asse Fault and Aachen Fault) (Cambier G. & Dejonghe L., 2010).
The Midi Fault is a major thrust which extends laterally from Germany to England of Variscan age. The fault has a low angle dip which flattens at depth and roots into a detachment underlying the thick terrigenous sequence of the Variscan frontal units. The eastern continuation of the Midi Fault from Belgium to Germany is the Aachen Fault (Keppie J.D. 1994).
Northern Variscan thrust faults
The known northern limit of the Varsican deformation corresponds to these thrust faults (the Northern Varsican thrust faults). These are therefore used at GIS level for this purpose, rather than being a conceptual SF limit.
Malmedy fault system
Bouhouille Fault
The importance of the Bouhouille Fault depends on the relevance of the Aguesses-Asse Fault (see ScopeNote of Aguesse-Asse Fault). If the Asse Fault is interpreted as the eastward continuation of the Aguesse Fault and not as an individual fault, than the Bouhouille Fault plays an important role in explaining the transverse movement between the Aguesses and Asse faults (GeoConnect³d).
The Bouhouille Fault is a NNW-SSE oriented sinistral transverse fault of post-Variscan age. Towards the south it continues as the Evegnée Fault (Cambier G. & Dejonghe L. 2010; Barchy L. & Marion J. (2000).
Evegnée Fault
Verviers Fault
Ostende Fault
Xhoris Fault
The Xhoris Fault is a thrust-type fracture of Variscan age that affects two major units of Belgian regional geology. The western segment disrupts the Eifelian-Frasnian formations of the eastern border of the Dinant Synclinorium. While the eastern segment displaces the Cambrian-Ordovician rocks of the Stavelot Massif (Cambier G. & Dejonghe L., 2010).
Mouhy Fault
Walhorn Fault
The Walhorn Fault is a thrust fracture of Variscan age that comprises of different fault segments, each named differently depending on their geography, from east to west: the Walhorn, Renoupré, Haute-Folie and Pépinster Faults. The fault bounds the northern part of the Goé Unit, a small inner thrust sheet of the Vesdre Nappe (Cambier G. & Dejonghe L., 2010).
Pepinster Fault
Monty Fault
Theux Fault
It marks the boundary between the autochthonous area of the Theux Window and the surrounding allochthonous thrust nappe. In the north, the north-dipping Theux Fault is indicated to connect with the south-dipping Tunnel Fault, making the Theux-Tunnel Thrust to be considered as a junction between the Midi Fault in the west and the Aachen Fault in the east (Cambier G. & Dejonghe L., 2010).
The Theux Fault is a circle-shaped thrust fracture (window) which bounds the west, north and east sides of the Theux Window (Cambier G. & Dejonghe L., 2010).
Landenne Fault
The Landenne Fault is a steeply dipping reverse fracture with northward plunge. It marks the boundary between Silurian rocks of the Brabant Massif to the north and Lower Carboniferous rocks of the Namur Synclinorium to the south (Cambier G. & Dejonghe L., 2010).
Tektonikat e Shqiperise
Kontakt tektonik midis zonës tektonike Jonike dhe zonës tektonike Sazani
Tectonic Boundary in Albania
All named tectonic boundary objects that are located in Albania, are identified by an ID with the prefix „AL“ listed in the notation.
Fault in Albania, displayed in the HIKE European fault database.
Shkoder-Selimaj nappe boundary
Shkoder-Selimaj
Tektonike mbihypëse- Kontakt tektonik midis zonës tektonike të Alpeve dhe zonës tektonike Cukali
Kostenje-Çerenec Fault System
Kostenje-Çerenec
Mbulesore
Sebisht Fault
Sebisht
Tektonike afrovertikale, tektonike shariazhuese (mbulesore)
Kurbnesh Fault System
Kurbnesh
Mbihypese
Kruma Fault
Kruma
Tektonike afrovertikale
Arreni Fault
Arreni
Tektonike afrovertikale, tektonike paralele formacionale
Zogaj Fault
Zogaj
Cahani Fault
Cahani
Macukulli Fault
Macukulli
Tektonike afrovertikale, tektonike parakretake me karakter mbihypes
Kunora e Lures Fault
Kunora e Lures
Zall Gjoçaj Fault
Zall Gjoçaj
Merkurth Fault
Merkurth
Tektonike afrovertikale, tektonike strike-slip
Thirre Fault
Thirre
Perlat I Eperm Fault
Perlat I Eperm
Malaj Fault
Malaj
Mziu Fault
Mziu
Karme Fault
Karme
Sakati (Blerim) Fault
Sakati (Blerim)
Kulumri (Blerim) Fault
Kulumri (Blerim)
Kashnjeti Fault System
Kashnjeti
Bukmire Fault
Bukmire
Tektonike afrovertikale , tektonike parakretake me karakter mbihypes
Vucim-Cerem-Mali I Brovines Fault System
Vucim-Cerem-Mali I Brovines
Tektonike shariazhuese- Kontakt tektonik midis zones tektonike Gashi dhe zones tektonike Alpine
Seferece Fault
Seferece
Sulbica Subfault
Sulbica
Vrepcke Fault
Vrepcke
Borova Fault
Borova
Radanj Fault
Radanj
Tektonike afrovertikale formacionale, tektonike shariazhuese
Germenj Fault
Germenj
Tektonike mbulesore
Germenj Subfault
Germenj (1)
Mali I Marlules Fault
Mali I Marlules
Tektonike afrovertikale formacionale
Gjonçi Fault
Gjonçi
Tektonike afrovertikale formacionale, tektonike parakretake
Vithkuq Fault
Vithkuq
Tektonike afrovertikale, tektonike me karakter mbulesor
Shkoza Fault System
Shkoza
Kapshtica Fault
Kapshtica
Tektonike afrovertikale, tektonike paralele
Pirgu Fault
Pirgu
Kloça Fault
Kloça
Ostreni Fault System
Ostreni
Mbulesore, tektonike paralele dhe nderprerese
Trebisht Fault
Trebisht
Mali me Gropa Fault
Mali me Gropa
Tektonike afrovertikale, Bllok gravitativ
Burimas Subfault
Burimas
Bllok gravitativ
Guri I Bardhe Fault
Guri I Bardhe
Bena-Ura e Shenjte Fault 1
Bena-Ura e Shenjte
Bena-Ura e Shenjte Fault 2
Ukbibaj Subfault
Ukbibaj
Mazreku Subfault
Mazreku
Curraj I Eperm Fault System 2
Curraj I Eperm (2)
Raba e Ducajve Fault
Raba e Ducajve
Shllaku Fault
Shllaku
Mali I Thate Fault System
Mali I Thate
Velçani I Gores Fault
Velçani I Gores
Bulqize-Selishte Fault System
Bulqize-Selishte
Mbihypese, tektonike parakretake me karakter mbihypes
Vila Fault
Vila
Razem Fault System
Razem
Lepusha Fault
Lepusha
Vermosh Subfault
Vermosh
Mali I Grebenit Subfault
Mali I Grebenit
Gropat e Selces Subfault
Gropat e Selces
Mali I Cet Harushes Fault
Mali I Cet Harushes
Dragobia Fault
Dragobia
Mali I Bukoviqit Fault
Mali I Bukoviqit
Tamare Subfault
Tamare
Mali I Golishtit Fault 2
Mali I Golishtit (2)
Mbihypese, tektonikeme karakter mbihypese
Mali I Gjarprit Fault
Mali I Gjarprit
Mali I Kashticit Fault
Mali I Kashticit
Mbihypese, tektonikeme karakter mbihypes
Qafa e Barit Fault 1
Qafa e Barit
Repshaj Fault
Repshaj
Tektonike afrovertikale, tektonike qe nderpret formacionin kryq
Mali I Brodoshnices Fault
Mali I Brodoshnices
Boge Fault
Boge
Mali I Golishtit Fault 1
Mali I Golishtit (1)
Tektonike afrovertikale, tektonikeme karakter mbihypese
Mali I Shkelzenit Fault
Mali I Shkelzenit
Mali I Shenikut Fault
Mali I Shenikut
Mali I Vajushes Fault
Mali I Vajushes
Mali I Jezerces Fault 2
Mali I Jezerces (2)
Nikshi Fault
Nikshi
Mali I Zarzit Fault
Mali I Zarzit
Mali I Jezerces Fault 1 Subfault
Mali I Jezerces (1)
Qafa e Kloshit-Rogam Subfault
Qafa e Kloshit-Rogam
Qafa e Barit Fault 2
Mali I Radomires Fault
Mali I Radomires
Vucim Fault
Vucim
Brodoshnica Fault
Brodoshnica
Qafshtame-Rubik Fault System
Qafshtame-Rubik
Kastrati-Maja e Surtes Fault System
Kastrati-Maja e Surtes
Hoti Fault
Hoti
Mançurisht Fault System
Mançurisht
Toplana Fault 2
Toplana (2)
Fush Bualli Fault System
Fush Bualli
Berzeshta Fault
Berzeshta
Xhyra Fault
Xhyra
Spathar Fault
Spathar
Gurshpat Fault
Gurshpat
Kiri Fault
Kiri
Guri I Topit Fault System
Guri I Topit
Stravaj Fault
Stravaj
Verdova Fault
Verdova
Ulez Fault System
Ulez
Toplana Fault 1
Toplana (1)
Rubik-Rrenja e Zeze Fault System
Rubik-Rrenja e Zeze
Dushaj Fault
Dushaj
Mbihypese, tektonike parakretake formacionale
Kurora e Dardhes Fault
Kurora e Dardhes
Geraj Fault
Geraj
tektonike parakretake me karakter mbihypes
Iballe Fault
Iballe
Berishe e Vogel-Bugjon Fault
Berishe e Vogel-Bugjon
Nikolic-Gjergovic Fault System
Nikolic-Gjergovic
Mbihypese, tektonike me karakter srtike-slip
Arrza Fault
Arrza
Tektonike afrovertikale, tektonika paralele
Liraj-Biga e Shales Fault System
Liraj-Biga e Shales
Mali I Hekurave Fault
Mali I Hekurave
Tektonike afrovertikale, tektonike me karakter mbihypës
Troshani Fault
Troshani
Curraj I Eperm Fault 1
Curraj I Eperm (1)
Mali I Mardomit Fault
Mali I Mardomit
Ducaj Fault
Ducaj
Mali I Kurriles Fault 1
Mali I Kurriles (1)
Mali I Kurriles Fault 2
Mali I Kurriles (2)
Vajushi Fault 1
Vajushi (1)
Perroi I Rrjollit Subfault
Perroi I Rrjollit
Vajushi Fault 2
Vajushi (2)
Shkembi I Merturit Fault
Shkembi I Merturit
Palaj Subfault
Palaj
Brozhta Subfault
Brozhta
Rrajc-Sterblev Fault System
Rrajc-Sterblev
Miraka Fault
Miraka
Kuturman Fault
Kuturman
Mbihypese, tektonike shariazhuese
Gurakuq Fault
Gurakuq
Mbulesore, tektonike shariazhuese (mbulesore)
Fushe-Arrezi Fault System
Fushe-Arrezi
Levrushk-Kalimash Fault System
Levrushk-Kalimash
Dardha Fault System
Dardha
Voskopoja Fault
Voskopoja
Lavdari I Korçes Fault
Lavdari I Korçes
Lozhani Fault
Lozhani
Limanit Fault
Limanit
Gjylasi-Qerecke Fault
Gjylasi-Qerecke
Kurshove Fault
Kurshove
Qarishta Fault System
Qarishta
Qeleza Fault System
Qeleza
Kushneni Fault
Kushneni
Leskovik-Kukur-Elbasan-Milot-Oblik Nappe boundary
Leskovik-Kukur-Elbasan-Milot-Oblik
Tektonike mbulesore (shariazhuese)- Kontakt tektonik midis zonës tektonike Kruja dhe zonës tektonike Krasta
Cercka Fault
Cercka
Postenan Fault
Postenan
Leshnja Fault
Leshnja
Tektonike afrovertikale, tektonike paralele dhe terthore
Ulove Fault
Ulove
Ulove Subfault 1
Ulove (1)
Gurezeza Subfault
Gurezeza
Brashtan Fault System
Brashtan
Selita e Malit Fault
Selita e Malit
Zall-Bastar Subfault
Zall-Bastar
Mali I Kakariqit Fault
Mali I Kakariqit
Mali I Rencit Fault 1
Mali I Rencit (1)
Mener I Siperm Fault
Mener I Siperm
Sanxhak Fault
Sanxhak
Nezhan Fault
Nezhan
Tektonike afrovertikale, tektonike mbulesore
Letan Subfault
Letan
Trepsenisht Subfault
Trepsenisht
Bllok gravitativ, tektonike paralele
Mali I Rencit Fault 2
Mali I Rencit (2)
Leskovik-Poliçan-Liqeni i Banjes Large-Scale Fault System
Leskovik-Poliçan-Liqeni i Banjes
Dumre Fault System
Dumre
Mbihypje
Xhafaj-Mbolan Fault
Xhafaj-Mbolan
Xhafaj-Mbolan Fault 1
Xhafaj-Mbolan (1)
Zhulat-Picari Fault System
Zhulat-Picari
Vergo-Rusan Fault
Vergo-Rusan
Tektonike Diapirike
Delvina Fault
Delvina
Çepune-Senice Fault
Çepune-Senice
Zminec Fault
Zminec
Cerkovice Fault
Cerkovice
Krongj-Leshnice Fault
Krongj-Leshnice
Janicat-Qafe Leshnice Fault
Janicat-Qafe Leshnice
Dermish-Karroq Fault
Dermish-Karroq
Kodra Fault
Kodra
Toske-Mbjeshtove Fault System
Toske-Mbjeshtove
Velçan Fault System
Velçan
Vokopole Fault
Vokopole
Çarçove-Bodar-Poliçan-Turje Fault System
Çarçove-Bodar-Poliçan-Turje
Dragot-Sulove Fault
Dragot-Sulove
Topojan-Klos Fault
Topojan-Klos
Topojan-Klos Subfault
Tektonike afrovertikale-nderfaciale
Petran-Kukuçova Fault
Petran-Kukuçova
Selcka-Maja e Laducit Subfault
Selcka-Maja e Laducit
Golemaj-Bubsi Fault
Golemaj-Bubsi
Peshtan-Mezhgoran Fault
Peshtan-Mezhgoran
Beçisht Subfault
Beçisht
Caush-Janjar Fault System
Caush-Janjar
Vana-Lukova Fault
Vana-Lukova
Vergo-Tatzat Fault
Vergo-Tatzat
Tatzat Fault
Tatzat
Janjar Subfault
Janjar
Fushebardhe Fault
Fushebardhe
Çiflik Subfault
Çiflik
Bregas-Nivice Fault
Bregas-Nivice
Markat-Verva Fault
Markat-Verva
Sopiku Fault
Sopiku
Ksamil Subfault
Ksamil
Borsh-Bolene Fault System
Borsh-Bolene
Qeparo Fault
Qeparo
Krahesi i Siperm Fault System
Krahesi i Siperm
Ballsh Fault
Ballsh
Libohove Fault 1
Libohove (1)
Radat Subfault
Radat
Vllaho-Goranxi Subfault
Vllaho-Goranxi
Nivan Fault
Nivan
Asim Zeneli Subfault
Asim Zeneli
Glina Fault
Glina
Libohove Fault 2
Libohove (2)
Maja e Strokavecit Fault
Maja e Strokavecit
Maja e Kendrevices Fault
Maja e Kendrevices
Greshice Fault
Greshice
Bençe Fault
Bençe
Vau I Dejes-Selimaj Nappe boundary
Vau I Dejes-Selimaj
Tektonike shariazhuese- Kontakt tektonik midis zonave tektonike
Qafe Llogara Fault System
Qafe Llogara
Kontakt Tektonik Horst-Graben
Qafa e Brisarit Fault
Qafa e Brisarit
Kepi i Gjuhezes Subfault 1
Kepi i Gjuhezes (1)
Kepi i Gjuhezes Subfault 2
Kepi i Gjuhezes (2)
Kontakt tektonik midis zonës tektonike Jonike dhe zonës tektonike Kruja
Mali i Flamurit Subfault
Mali i Flamurit
Dhermi Subfault
Dhermi
Tektonike afrovertikale Horst-Graben
Zerqan-Surroj-Morine Nappe boundary
Zerqan-Surroj-Morine
Mbihypese, Tektonika paralele
Kulla e Zyberit Fault System
Kulla e Zyberit
Nimce Fault
Nimce
Tershana Fault
Tershana
Kolesjan Fault
Kolesjan
Turaj Fault
Turaj
Lume-Xhaferaj Fault
Lume-Xhaferaj
Gjallica Fault
Gjallica
Pobreg Fault
Pobreg
Tejdrini Fault
Tejdrini
Shtiqen Fault
Shtiqen
Gryke Noka Fault System
Gryke Noka
Selishta Fault
Selishta
Homesh Fault
Homesh
Tektonike afrovertikale, tektonike me karakter shariazhues (mbulesor)
Lukani Fault
Lukani
Sopoti Fault System
Sopoti
Poçest Fault
Poçest
Shariazh, tektonike shariazhuese me karakter mbulesor
Peshkopia Fault
Peshkopia
Shariazh, tektonike me karakter mbihypes
Fushe Bulqize Fault
Fushe Bulqize
Gjurasi Subfault
Gjurasi
Fushe Muhur Subfault
Fushe Muhur
Tektonike afrovertikale, tektonike shariazhuese me karakter mbulesor
Arapaj I Poshtem Subfault
Arapaj I Poshtem
Shqathi Subfault
Shqathi
Zimur Fault
Zimur
Kuc-Ramice Large-Scale Fault System
Kuc-Ramice
Ilias - Pilur Fault
Ilias - Pilur
Tektonike afrovertikale, ektonike paralele
Arianitasi Subfault
Arianitasi
Sinje Subfault
Sinje
Llakatund Fault
Llakatund
Mali I Vashes-Rohmisht-Strelce-Mali I Firtit-Guri I Bardhe-Rubik-Hajmel Nappe boundary
Mali I Vashes-Rohmisht-Strelce-Mali I Firtit-Guri I Bardhe-Rubik-Hajmel
Tektonike mbulesore (shariazhuese)- Kontakt tektonik midis zonës tektonike Krasta dhe zonës tektonike Mirdita
Bostani Fault System
Bostani
Cudhi-Kami Fault System
Cudhi-Kami
Selita Fault
Selita
Spiten Fault
Spiten
Manati Fault System
Manati
Manati Fault
Manati (1)
Nenshati Fault
Nenshati
Mali i Merqies Fault
Mali i Merqies
Mërqi Fault
Mërqi
Lencka Fault
Lencka
Kamniku Fault 1
Kamniku (1)
Kamniku Fault 2
Kamniku (2)
Tektonike afrovertikale, bllok brenda formacionit
Benjeza Subfault
Benjeza
Ostrovica Fault System
Ostrovica
Alloktoni I Devollit Fault 1
Alloktoni I Devollit (1)
Mali I Lenies Fault
Mali I Lenies
Lenie Fault
Lenie
Alloktoni I Devollit Fault 2
Alloktoni I Devollit (2)
Mali I Oparit Fault
Mali I Oparit
Ostrovica Fault
tektonike paralele dhe terthore
Gurekuq Fault
Gurekuq
Gurakuqi Subfault
Gurakuqi (1)
tektonike nderprerese
Kurtes Fault System
Kurtes
Trebicka Fault
Trebicka
Propanik Fault System
Propanik
Bena Fault
Bena
Shengjin I Madh
Labinot Mal Fault
Labinot Mal
Nenishat
Qafa e Selites Fault System
Qafa e Selites
Tectonic Boundary in the Pannonian Basin
Tectonic Boundary in Denmark
All named tectonic boundary objects that are located (at least partly) in Denmark, are identified by an ID with the prefix „DK“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Denmark, displayed in the HIKE European fault database.
Tectonic Boundary in France
All named tectonic boundary objects that are located (at least partly) in France, are identified by an ID with the prefix „FR“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in France, displayed in the HIKE European fault database.
All named tectonic boundary objects that are located (at least partly) in Lithuania, are identified by an ID with the prefix „LT“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Lithuania displayed in the HIKE European fault database.
Tectonic boundary in Lithuania
Tektoninės ribos Lietuvoje
West Lithuanian Fault Domain
Faults were identified by 2D (predominantly) and 3D seismic, well data, supported by potential fields data. West Lithuanian fault domain is situated in the west part of Lithuania, from the Baltic sea to Pasvalys town, Nevezis river, Kaunas city and Lazdijai town. Faults of the Domain are identified in crystalline basement and penetrate the Lower Paleozoic sedimentary cover. The faults could be traced up to Lower Devonian Gragzdai Group (Early Pragian).
Lūžiai nustatyti 2D (daugiausiai) ir 3D seisminės žvalgybos, gręžinių ir potencialių laukų duomenimis. Vakarų Lietuvos lūžių domeinas apima vakarinę Lietuvos dalį, nuo Baltijos jūros iki Pasvalio miesto, Nevėžio upės, Kauno miesto ir Lazdijų miesto. Lūžių domeiną sudarantys lūžiai išskiriami kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Vakarų Lietuvos lūžių Domeinas
Gubriai Fault Chain
Gubriai fault chain comprises N-S and W-E oriented faults. They extend from the river Jura to Griniai village. Faults are of reverse type, they have been identified by 2D seismic and well data.
Grandinę sudaro lūžiai orentuoti Š-P ir V-R kryptimis besitęsiantys nuo Jūros upės iki Grinių gyvenvietės. Lūžiai yra antsprūdžio tipo, išskirti 2D seisminės žvalgybos ir gręžinių duomenimis.
Gūbrių lūžių grandinė
Mazeikiai-Telsiai Fault Set
The fault set comprises predominantly rerverse type faults, identified by 2D and 3D seismic and well data. Fault set is located in the North west part of Lithuania, in the North the faults strike from Skuodas town to Mazeikiai town, in the South - from the coast of Baltic sea, crosses Kretinga town and Siauliai city, and continues to Pakruojis town. Faults of the fault set are identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover. The faults could be traced up to Lower Devonian Gragzdai Group (Early Pragian).
Lūžių grupę sudaro ansprūdžio tipo lūžiai, išskirti seisminės 2D ir 3D žvalgybos ir gręžinių duomenimis. Mažeikių-Telšių lūžių grupė yra šiaurės vakarinėje Lietuvos dalyje, šiaurėje lūžiai transuojami nuo Skuodo miesto iki Mažeikių miesto, pietuose nuo Baltijos jūros kranto, kerta Kretingos ir Šiaulių miestus ir tęsiasi link Pakruojo miesto. Lūžiai išskiriami kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Mažeikių - Telšių lūžių grupė
Telsiai Fault Zone
Telsiai fault zone is oriented in W-E direction and is asigned to reverse fault type. The amplitude exceeds 300 m; the total length of onshore Telsiai fault zone is up to 270 km.The NE-SW faults are dipping at the angles 60-80o. The fault zone was identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover. The faults could be traced up to Lower Devonian Gragzdai Group (Early Pragian). The fault zone extends from the Baltic sea, through Palanga town, Plunge town, Telsiai town, crosses Siauliai city and continues to Birzai town.
Telšių lūžių zona yra orientuota V-R kryptimi, ji tęsiasi nuo Baltijos jūros pakrantės, pro Palangos miestą, Plungės miestą ir Telšių miestą, kerta Šiaulių miestą ir tęsiasi link Biržų miesto. Lūžių zonos lūžiai yra antstūmio tipo. Telšių lūžių zonos amplitudė viršija 300 m, o jos žemyninės dalies ilgis siekia 270 km. Lūžiai išskiriami kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Telšių lūžių zona
Gruzdziai Fault
Gruzdziai fault is oriented in SW - NE direction. The fault strikes from the Gruzdziai village and continues towards direction of Latvia, it croses Musa river along the way. The type of the fault is assigned to reverse faults type. It has been identified by 2D seismic survey data and by interpretation of the magnetic and gravity anomalies.
Gruzdžių lūžis yra orentuotas PV-ŠR kryptimi. Jis tęsiasi nuo Gruzdžių gyvenvietės link Latvijos teritorijos, pakeliui kertant Mūšos upę. Gruzdžių ansprūdžio tipo lūžis yra nustatytas 2D seisminės žvalgybos duomenimis ir interpretuojant gravitacinės ir magnetinės žvalgybos duomenis.
Gruzdžių lūžis
Tryskiai Fault
Tryskiai fault is oriented in S - N direction. Tryskiai fault strikes from the Virvyte river and continues towards direction of Venta town. The type of the fault is reverse fault. It has been identified by 2D seismic survey data. The fault was identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover. The faults could be traced up to Lower Devonian Gragzdai Group (Early Pragian).
Tryškių lūžis yra orentuotas P-Š kryptimi ir tęsiasi nuo Virvytės upės link Ventos miesto. Šis lūžia yra priskiriamas antsprūdžio tipo lūžiams. Lūžis nustatytas naudojant 2D seisminės žvalgybos duomenis. Tryškių lūžis yra išskiriamas kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Tryškių lūžis
Klaipeda Fault
Klaipeda fault is oriented in SW - NE direction. The fault strikes from coast of Baltic sea to Palanga town and continues to direction of Salantai village. Fault is asigned to reverse faults type. It has been identified by 2D seismic survey and well data. The fault was identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover. The faults could be traced up to Lower Devonian Gragzdai Group (Early Pragian).
Klaipėdos lūžis - orentuotas PV - ŠR kryptimi, jis tęsiasi nuo Baltijos jūros pakrantės, pro Palangos miestą link Salantų gyvenvietės. Lūžis yra priskiriamas prie ansprūdžio tipo lūžių. Lūžis nustatytas 2D seisminės žvalgybos ir gręžinių duomenimis. Klaipėdos lūžis yra išskiriamas kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Klaipėdos lūžis
Mazeikiai Fault
Mazeikiai fault is oriented in SW - NE direction. Mazeikiai fault strikes from Tryksiai village, through Mazeikiai town and continues to Venta river. The amplitudes ranges from 25 to 50 meters. The fault inclines to the north, it is assigend to reverse faults type. It has been identified by 2D seismic and well data. The fault was identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover. The faults could be traced up to Lower Devonian Gragzdai Group (Early Pragian).
Mažeikių lūžis orentuotas V-ŠR kryptimi tęsiasi nuo Trikšlių gyvenvietės, pro Mažeikių miestą link Ventos upės. Lūžio amplitudė kaiti - vidutiniškai yra apie 25 m, vietomis padidėja iki 50 m. Lūžis yra antspūdžio tipo palinkęs šiaurės kryptimi. Lūžis nustatytas 2D seisminės žvalgybos ir gręžinių duomenimis. Mažeikių lūžis yra išskiriamas kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Mažeikių lūžis
Akmene Fault
Akmene fault is oriented in NW - SE - NE direction. Fault strikes from Skuodas town, to Seda village and continues to Naujoji Akmene town. The fault continues as Pape fault zone to the Latvian teritory. This fault is asighn to reverse faults type. It has been identifiedby 2D seismic survey and well data.The fault was identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover. The fault could be traced up to the Carboniferouse.
Akmenės lūžis yra orentuotas ŠV-PR-ŠR kryptimi. Lūžis tęsiasi nuo Skuodo miesto, pro Sedos miestelį link Naujosios Akmenės miesto. Lūžis vakarų Latvijoje susijungia su Papės lūžių zona. Jis yra antsprudžio tipo. Lūžis nustatytas 2D seisminės žvalgybos ir gręžinių duomenimis. Akmenės lūžis yra išskiriamas kristaliniame pamate ir nuosėdinėje dangoje iki karbono.
Akmenės lūžis
Rietavas Fault SubDomain
Reverse faults are oriented in SW-NE direction. Faults are situated between Kliete river and Rietavas town. Faults are identified in crystalline basement and penetrate the Lower Paleozoic sedimentary cover up to Lower Devonian Gragzdai Group (Early Pragian). They have been identified by 2D seismic and well data.
Lūžiai yra orentuoti PV-ŠR kryptimi. Lūžiai yra išsidėstę tarp Klietės upės ir Rietavo miesto. Lūžiai išskiriami kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis). Lūžiai išskirti 2D seisminės žvalgybos ir gręžinių duomenimis.
Rietavo lūžių Sub-Domeinas
Gargzdai Fault Chain
NNE-SSW striking Fault Chain consists of a set of reverse faults. The fault chain extend from Agluonenai village to Gargzdai town. It consists of major Gargzdai fault zone and related sattelite faults. The amplitudes range from a few dozen to 100 m. The NE-SW faults set shows rather simple compresional geometries dipping to the west at the angles 70-80o. Faults were identified by 2D and 3D seismic and well data. Faults are identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover up to Lower Devonian Gragzdai Group (Early Pragian ).
Lūžių grandinę sudaro antsprūdžio tipo lūžiai, orientuoti ŠŠR - PPV ir ŠR-PV kryptimis. Lūžiai yra išsidėstę nuo Agluonėnų gyvenvietės link Gargždų miesto. Lūžių grandinė vakaruose ribojasi su Baltijos jūra ir rytuose ribojasi su Veiviržo upe. Gargždų lūžių grandinę sudaro pagrindinė Gargždų lūžių zona ir kiti susiję lūžiai. Gargždų lūžių grandinę sudarančių lūžių amplitudė kinta nuo kelių dešimčių iki 100 metrų. Gargždų lūžių grandinės lūžiai nustatyti 2D ir 3D seisminės žvalgybos ir gręžinių duomenimis. Lūžiai išskiriami kristaliniame pamate ir nuosėdinėje dangoje iki apatinio devono Gargždų Serijos (ankstyvaisis Pragis).
Gargždų lūžių grandinė
East Lithuanian Fault Domain
The East Lithuanian fault domain is dominated by alternation of distinct NNE-SSW and W-E trending faults' chains, coinciding with magnetic and gravity anomalies implying lenticular tectonic fabric of the basement rocks. The internal structure of the ELD is composed by a system of thrust-folds dipping to the west at low angles. East Lithuanian Fault Domain is located in eastern part of Lithuania. In the west from the fault domain there are Pasvalys town, Nevezis river, Kaunas city and Lazdijai town, in the east - Latvia and Belarus boundaries.
Rytų Lietuvos lūžių domeiną sudaro ŠŠR-PPV ir V-R kryptimis besitęsiančios lūžių grandinės, išskirtos pagal gravitacines ir magnetines anomalijas, gerai atspindinčias kristalinio pamato lentikuliarinę tektoninę sandarą. Domeino vidinei sandarai būdinga antstūmių-raukšlių sistema, nedideliu kampu palinkusi vakarų kryptimi. Rytų Lietuvos lūžių domeinas yra rytinėje Lietuvos dalyje, jis vakaruose ribojasi su Pasvalio miestu, Nevėžio upe, Kauno miestu ir Lazdijų miestu, ir rytuose tęsiasi link Latvijos ir Baltarusijos sienų.
Rytų Lietuvos lūžių domeinas
South-East Lithuanian Fault Chain
The fault chain consist of W-E and NNE-SSW oriented faults of the crystalline basement, identified by interpretation of the magnetic and gravity anomalies. The North-Western part of chain is located in vicinity of Kaunas city, the Eastern part - in vicinity of Vilnius city, and the Southern part - in vicinity of Druskininkai town.
Pietryčių Lietuvos lūžių grandinę sudaro V- R ir ŠŠR- PPV tįsos kristalinio pamato lūžiai. Šiaurės vakaruose lūžių grandinės dalis ribojasi su Kauno miestu, rytuose - su Vilniaus miestu, o pietuose su Druskininkų miestu. Lūžiai išskirti gravitacinės ir magnetinės žvalgybos duomenimis.
Pietryčių Lietuvos lūžių grandinė
NNE-SSW trending SubFaults
These NNE-SSW oriented faults of the crystalline basement are identified by interpretation of gravity and magnetic anomalies. In the North-West fault chain there is Kaunas city, in the East - Vilnius city and in the South - Druskininkai town.
Lūžiai yra antsprūdžio tipo, orientuoti ŠŠR - PPV kryptimi, nustatyti gręžinių, gravitacinės ir magnetinės žvalgybos duomenimis. Šiaurės vakaruose lūžių grandinė ribojasi su Kauno miestu, rytuose su Vilniaus miestu ir pietuose su Druskininkų miestu.
ŠŠR - PPV krypties tįsos sub-lūžiai
W-E trending SubFaults
These W-E oriented faults of the crystalline basement are identified by interpretation of the magnetic and gravity anomalies. The North-Western part of chain is located in vicinity of Kaunas city, the Eastern part - in vicinity of Vilnius city, and the Southern part - in vicinity of Druskininkai town.
Lūžiai orientuoti V-R kryptimi, išskirti kritaliniame pamate gravitacinės ir magnetinės žvalgybos duomenimis. Šiaurės vakaruose lūžių grandinė ribojasi su Kauno miestu, rytuose su Vilniaus miestu ir pietuose su Druskininkų miestu.
V-R krypties tįsos sub-lūžiai
Ignalina Fault Chain
Faults are oriented in SW-NE direction. They are reverse type faults, located around the Visaginas town. They have been identified with seismic survey data and by interpretation of gravity and magnetic anomalies and well data. The faults were identified in crystalline basement and penetrate Lower Paleozoic sedimentary cover.
Ignalinos lūžių grandinės lūžiai yra PV- ŠR krypties, nustatyti aplink Visagino miestą. Šie lūžiai nustatyti seisminės žvalgybos, gravitacinės ir magnetinės žvalgybos ir gręžinių duomenimis. Lūžiai išskiriami kristaliniame pamate ir nuosėdinėje dangoje.
Ignalinos lūžių grandinė
Zarasai-Polockas Fault system
W-E trending fault system of the crystalline basement is identified by interpretation of the magnetic and gravity anomalies. Fault system is in the Northeast Lithuania, between Zarasai, Panevezys, Ramygala and Ignalina towns.
V-R kryptimi orientuoti kristalinio pamato lūžiai, nustatyti gravitacinės ir magnetinės žvalgybos duomenimis. Lūžių sistema yra šiaurės rytinėje Lietuvos dalyje, tarp Zarasų, Panevėžio, Ramygalos ir Ignalinos miestų.
Zarasų-Polocko lūžių sistema
Polockas Fault
Polockas fault is oriented in W-E direction and identified as share zone, inclined to the north at the angle 25o. The dislocation amplitude at crystaline basement is up to 50 m. Polockas fault strikes from Ramygala town to the Ignalina town and continues to Belarus. The fault has been identified by interpretation of the magnetic and gravity anomalies.
Polocko lūžis yra V-R krypties, antsprūdžio tipo, pasviręs į šiaurę 25o laipsnių kampu. Kristaliniame pamate dislokacijų amplitudė siekia 50 metrų. Šis lūžis trasuojamas nuo Ramygalos miesto, pro Ignalinos miestą link Baltarusijos teritorijos. Lūžis nustatytas gravitacinės ir magnetinės žvalgybos ir gręžinių duomenimis.
Polocko lūžis
Zarasai Fault
Fault in the crystalline basement is oriented in W-E direction. It is nearly vertical. The strike-slip movements are preferred along the fault. It strikes from the city of Panevezys to the Zarasai town and continues to Latvia. The fault has been identified by interpretation of gravity and magnetic anomalies.
Lūžiai orientuoti V-R kryptimi, išskirti kritaliniame pamate. Jis tęsiasi nuo Panevėžio miesto pro Zarasų miestą link Latvijos teritorijos. Lūžis nustatytas gravitacinės ir magnetinės žvalgybos duomenimis.
Zarasų lūžis
Mid-Lithuanian Share Zone
The first-order tectonic element of the crystalline basement is the N-S trending Middle Lithuanian share zone separating Western Lithuanian domain and East Lithuanian Domain, it also marks a considerable offset of the Moho (amplitude ~10 km). Middle Lithuanian share zone extends from Lazdijai town, through Kaunas and Panevezys cities to Joniskis town.
Tai stambiausio rango kristalinio pamato tektoninių šlyties deformacijų zona, skirianti Rytų ir Vakarų Lietuvos domeinus. Zona stebima ir Moho paviršiaus deformacijomis (iki 10 km amplitudės). Ši zona yra vidurio Lietuvoje ir tęsiasi šiaurės-pietų kryptimi. Vidurio Lietuvos šlyties zona tęsiasi nuo Lazdijų miesto, per Kauno ir Panevėžio miestus link Joniškio miesto.
Vidurio Lietuvos šlyties deformacijų zona
Zaltiniai Fault Chain
Faults are oriented in E-W and NW-SE directions. Faults strike to the South and South-East from Sakiai town. They have been identified by 2D siesmic data and by interpretation of the magnetic and gravity anomalies and well data. These faults are reverse type.
Lūžiai orentuoti R-V ir ŠV-PR kryptimis. Žaltinių lūžių grandinę sudarantys lūžiai trasuojami pietuose - pietryčiuose nuo Šakių miesto. Jie nustatyti 2D seisminės žvalgybos, gravitacinės ir magnetinės žvalgybos ir gręžinių duomenimis. Šie lūžiai yra antsprūdžio tipo.
Žaltinių lūžių grandinė
Vaskai Fault
Vaskai fault is oriented in SW-NE direction, it is identified in the crystalline basement and penetrates the entire Devonian strata with an amplitude up to 25 m. Some segments of fault were identified by 2D seismic survey data, some - by gravity and magnetic survey and well data. Fault strikes from Pakruojis town, through Birzai town and continues to Latvia teritory.
Vaškų lūžis yra PV-ŠR krypties ir transuoja nuo Pakruojo miesto, pro Biržų miestą link Latvijos teritorijos . Šie lūžiai yra antsprūdžio tipo. Dalis šių lūžių yra nustatyta seisminės žvalgybos duomenimis, kita dalis - gręžinių, gravitacinės ir magnetinės žvalgybos duomenimis.
Vaškų lūžis
All named tectonic boundary objects that are located (at least partly) in Saxony-Anhalt, are identified by an ID with the prefix „DE-ST“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID. In addition, as the concepts are also located in Germany, they may have an additional ID in form of „DE“ referring to a national Germany-wide dataset.
Representation of an interpreted tectonic boundary in Saxony-Anhalt as displayed in the HIKE European fault database
Tectonic Boundary in Saxony-Anhalt
Repräsentation einer interpretierten tektonischen Grenzfläche in Sachsen-Anhalt.
Tektonische Grenzfläche in Sachsen-Anhalt
Fault zones of the Calvörde Block
The Calvörde Block in the south and southwest of the Altmark area forms a basement uplift of Late Cretaceous age. It is covered by older Mesozoic rocks (Triassic), which were uplifted and folded in a flexure above a large basement fault, the Gardelegen Fault, respectively. To the south the Haldensleben and Wittenberg Fault zones separate the Calvörde Block against the Flechtingen High.
Die Scholle von Calvörde im Süden und Südwesten der Altmark bildet eine Sockelerhebung, die sich in der späten Kreidezeit heraushob. Sie ist von älteren mesozoischen Gesteinen (Trias) bedeckt, die in einer Flexur über einer großen Sockelstörung, der Gardelegen-Überschiebung, emporgehoben und gefaltet wurden. Im Süden trennen die Haldensleben und Wittenberg Überschiebungen den Calvörde-Block vom Flechtinger Höhenzug.
Störungszonen der Scholle von Calvörde
Dannefeld Fault Zone
The Dannefeld fault zone forms a reverse reactivated normal fault in Permian to Mesozoic strata of the western Calvörde Block. Activity along the Dannefeld fault zone was strongly associated with halokinetic movements in the Zechstein salt thus resulting in the formation of the Dannefeld diapir.
Die Dannefeld-Verwerfungszone bildet eine revers-reaktivierte Abschiebung in der permischen bis mesozoischen Schichtenfolge der Scholle von Calvörde. Die Aktivität entlang der Dannefeld Störungszone war stark mit halokinetischen Bewegungen im Zechstein-Salz verbunden, was zur Bildung des Dannefeld Diapirs führte.
Dannefeld-Störungszone
Dannefeld Fault
Crestal Graben of the Dannefeld salt structure
The Scheitelgraben Dannefeld forms a collaps structure on top of the Dannefeld diapir.
Der Scheitelgraben Dannefeld bildet eine Einbruchstruktur im Dachbereich des Salzstocks Dannefeld.
Scheitelgraben der Salzstruktur Dannefeld
Gardelegen Fault Zone
The NW-SE-striking and SW-dipping, 50 km long Gardelegen fault is one of the most important basement thrusts (‘Central German Main Escarpments’). While a maximum vertical displacement of 3.5 km (corresponding to 5 km fault offset) is detectable at the Base Zechstein horizon, fault offsets in the sedimentary cover (Top Zechstein) are low (< 200 m) and deformation is substituted by flexural folding. These huge offset variations furthermore coincide with thickness variations of the Zechstein salt across the Gardelegen fault. That observation indicates that salt migrated from the hanging wall to the footwall, which may was associated with thrusting and folding equivalent to ‘trishear’ fault-propagation folding (Erslev, 1991; Hardy and Ford, 1997). In the west, the fault zone abruptly starts with large offsets. A 10 km wide, long-wavelength foreland syncline comprises a uniform basin fill of Early Triassic-Late Jurassic strata overlain by a thick Late Cretaceous (Coniacian to Santonian) succession. Farther east, Late Jurassic-Early Cretaceous strata is absent and the foreland syncline became narrower. Fault offsets slightly decrease, where the fault trace converges towards the Haldensleben fault in a complex ‘en echelon’ pattern of fault zones (Brehm fault and Burg-Reuden-fault).
Die NW-SE-streichende und SW-einfallende, 50 km lange Gardelegen-Überschiebung ist eine der wichtigsten Sockel-Überschiebungen („Mitteldeutsche Hauptabbrüche“) Mitteldeutschlands. Während die Basis Zechstein bis zu 3,5 km relativ zum nördlichen Vorland gehoben ist (entspricht ca. 5 km Störungsversatz), sind Versätze in den mesozoischen Einheiten relativ gering (<200 m) und durch eine großräumige Flexur vertreten. Diese enormen Versatzvariationen gehen mit Mächtigkeitsschwankungen der Zechstein-Salze über die Gardelegen-Überschiebung einher. Diese Beobachtung deutet darauf hin, dass Salz vom Hangenden zum Liegenden migrierte. Im Westen beginnt die Verwerfungszone abrupt mit großen Versatzbeträgen. Eine 10 km breite, langwellige Mulde im Vorland zeigt einheitliche Beckensedimente der frühen Trias bis zum späten Jura. Diese werden einer mächtigen Abfolge der spätkretazischer Sedimente (Coniacian bis Santonian) überlagert. Weiter östlich fehlen Schichten des späten Jura und der frühen Kreide und die Vorland-Mulde wird deutlich kurzwelliger. Die Störungsversätze nehmen leicht ab, wobei die Störungsspur in einem komplexen „en echelon“-Muster von Einzelstörungen (Brehm Störungszone und Burg-Reuden Störungszone) gegen die Haldensleben Überschiebung konvergiert.
Gardelegen-Überschiebung
Gardelegen Thrust
Abbruch von Gardelegen
Fault zones of the Subhercynian Basin
The Subhercynian Depression is that area of Saxony-Anhalt, which is located between the basement uplifts of the Flechtingen High and the Harz Mountains. To the north (Flechtingen High) its border forms the mostly continuous transition from Mesozoic and Late Palaeozoic (Zechstein) strata to Palaeozoic crystalline and sedimentary rocks of the Flechtingen High. To the south the northern border fault of the Harz Mountains and steep-dipping Zechstein strata associated with basement faulting form the structural border of the Subhercynian Depression. The internal structure of the Subhercynian Depression is mostly characterized by NW-SE-trending fault zones, which are in parts accompanied with the intrusion of mechanically weak (Zechstein) salt (e.g. salt structure ‘Oberes Allertal’, ‘Offleben-Oschersleben-Staßfurter Salzsattel’), local thin-skinned anticlines (e.g., ‘Quedlinburger Sattel’, long-wavelength fault-related folds and deep synclines. Although the entire Subhercynian Depression underwent uplift in Late Mesozoic to Cenozoic times, relicts of older (Mesozoic) strata indicate a similar structural evolution like in the Altmark area further north. The Subhercynian Depression can be subdivided into several smaller blocks [Martiklos et al., 2001.]
Das Subherzyne Becken ist eine geologische Großstruktur im Gebiet von Sachsen-Anhalt, das sich zwischen den Sockelaufbrüchen des Flechtinger Höhenzugs im Norden und des Harzes im Süden befindet. Im Norden ist seine Grenze meist durch den gering versetzten, kontinuierlichen Übergang von Schichten des Mesozoikums und des späten Paläozoikums (Zechstein) zu kristallinen und sedimentären Gesteinen des Paläozoikums des Flechtinger Höhenzugs definiert. Im Süden bildet die Harznordrandstörung und die mit ihr assoziierten steil einfallenden Permotriassischen Schichten die strukturelle Grenze des Subherzynen Beckens. Die innere Struktur des Subherzynen Beckens ist hauptsächlich durch NW-SE-streichende Störungszonen charakterisiert, die teilweise mit dem Aufstieg von mechanisch weichen Einheiten, den Zechstein-Salzen einhergehen (z. B. Salzstruktur 'Oberes Allertal', 'Offleben-Oschersleben-Staßfurter Salzsattel'). Lokal existieren enge Detachment Faulten (z. B.' Quedlinburger Sattel ', langwellige störungsbedingte Falten und tiefe Synklinalen). Obwohl das gesamte Subherzyne Becken im späten Mesozoikum bis ins Känozoikum emporgehoben wurde, weisen Relikte älterer (mesozoischer) Schichten auf eine ähnliche strukturelle Entwicklung wie im weiter nördlich gelegenen Altmark-Gebiet hin.
Störungszonen des Subherzynen Beckens
Westerhausen Fault Zone
The Westerhausen fault zone forms an major basement fault in the western Subhercynian Basin, which is associated with strong halokinetic movements.
Die Westerhausen Störung bildet eine bedeutende Sockelstruktur im westlichen Subherzynen Becken, die mit bedeutenden halokinetischen Bewegungen einherging.
Westerhausen-Störungszone
Westerhausen Fault
Quedlinburg Fault Zone
The Quedlinburg Fault Zone forms a NW-SE-striking anticline in the eastern part of the Subhercynian Basin. It separates the Halberstadt and Blankenburg Synclines against each other.
Der Quedlinburger Störungszone bildet eine NW-SE-streichende Antiklinalstruktur im östlichen Subherzynen Becken. Die abgescherte Antiklinalstrukture separiert die Halberstädter und Blankenburger Mulde gegeneinander.
Quedlinburger Störungszone
Quedlinburg Fault
Quedlinburger Sattel
Vienenburg-Schauen Fault Zone
The Vienenburg-Schauen fault zone is a thin-skinned thrust fault and forms the western part of the Westerhausen fault zone.
Die Vienenburg-Schauen Störungszone ist eine abgescherte Überschiebungsstruktur und bildet den westlichen Abschnitt der Westerhausen Störungszone.
Vienenburg-Schauen-Störungszone
Harli-Störungszone
Aschersleben Fault Zone
The Aschersleben fault forms a NW-SE trending basement fault accompanied by halokinesis. The northern basement block is raised approx. 1 km compared to the southern one. In the uppermost crest of the structure halokinetic structures (Aschersleben salt structure) occur, which are accompanied with subrosion sinks, some of which filled with thick tertiary sediments.
Die Ascherslebener Störung bildet eine markante NW-SE streichende, durch Halokinese begleitete Sockelstörung. Der nördliche Sockelblock ist gegenüber dem südlichen markant um ca. 1 km angeboben. Im Dachbereich der Struktur treten vermehrt halokinetische Strukturen (Ascherslebener Salzsattel) und Subrosionssenken auf, die zum Teil mit mächtigen tertiären Sedimenten gefüllt sind.
Ascherslebener-Störungszone
Aschersleben Fault
Schönebeck Graben
The Schönebeck Graben forms an extensional fault zone on the Weferlingen Block.
Der Schönebecker Graben bildet eine extensionale Störungszone im Bereich der Weferlinger Scholle.
Schönebecker Graben
Halberstadt Fault Zone
The Halberstadt fault zone forms a NW-SE trending fault zone in the Subhercynian Basin, which separates the central basin area from the deep synkinematic Cretaceous synclines of the Harz foreland.
Die Halberstadt Störungszone bildet eine NW-SE streichende Störungszone im Subherzynen Becken, die den zentralen Beckenbereich von den tiefen synkinematischen Kreidemulden des direkten Harzvorlandes trennt.
Halberstadt-Störung
Halberstadt Fault
Köthen-Bitterfeld Fault Zone
The Köthen-Bitterfeld fault zone forms a NW-SE trending fault zone in the central area of the Halle-Wittenberg Block.
Die Köthen-Bitterfeld Störungszone bildet eine NW-SE streichende Störungszone im Zentralbereich der Halle-Wittenberg Scholle.
Köthen-Bitterfeld-Störungszone
Köthen-Bitterfeld Fault
Zörbig Fault Zone
The Zörbig fault zone forms a NW-SE trending fault zone in the border area of the Halle-Wittenberg Block.
Die Zörbiger Störungszone bildet eine NW-SE streichende Störungszone im Grenzbereich der Halle-Wittenberg-Scholle.
Zörbiger Störungszone
Zörbig Fault
Bitterfeld Fault Zone
The Bitterfeld fault zone forms a NW-SE trending fault zone in the border area of the Halle-Wittenberg Block. It forms the southeastern part of the Köthen-Bitterfeld fault zone.
Die Bitterfeld Störungszone bildet eine NW-SE streichende Störungszone im Grenzbereich der Halle-Wittenberg-Scholle. Sie bildet das südöstliche Teilglied der Köthen-Bitterfelder Störungszone.
Bitterfelder Störungszone
Bitterfeld Fault
Grimschleben-Roschwitz Fault Zone
The Grimschleben-Roschwitz fault zone is a NE-SW to north-south trending fault zone in the southeastern Subhercynian Basin.
Die Grimschleben-Roschwitz Störungszone ist eine NE-SW bis nahezu Nord-Süd streichende Störungszone im südöstlichen Subherzynen Becken.
Grimschleben-Roschwitz-Störungszone
Grimschleben-Roschwitz Fault
Allertal Fault Zone
The Allertal Fault separates the Weferlingen Block in the north to the Lappwald Block in the south. Although fault kinematics of the Allertal Fault are still matter of debate [Best and Zirngast, 2000; Stottmeister et al., 1998], it can be summarized to form a Late Triassic/Late Jurassic-Early Cretaceous high-offset (> 2.5 km) normal fault, which probably formed as an extensional detachment fault and later underwent mild contraction and inversion.
Die Allertalstörung trennt den Weferlingen Block im Norden vom Lappwald Block im Süden. Obwohl die Störungskinematik der Allertalstörungszone immer noch umstritten ist [Best und Zirngast, 2000; Stottmeister et al., 1998], kann zusammengefasst werden, dass diese als flache Abschiebung mit hohem Versatz (> 2,5 km) während der späten Trias und der späten Jura-frühen Kreidezeit ausgebildet wurde. Während der späten Kreide erfuhr sie eine schwache Einengung und Reaktivierung als Aufschiebung.
Allertal-Störungszone
Allertal Fault
Störungszone Oberes Allertal
Ummendorf-Allertal Fault Zone
The Ummendorf-Allertal fault zone forms a E-W-trending extensional fault zone on the Weferlingen Block.
Die Ummendorf-Allertal Störungszone bildet eine Ost-West-streichende Grabenstruktur im Bereich der Weferlinger Scholle.
Ummendorf-Allertal-Störungszone
Ummendorf Graben
The Ummendorf Graben forms a collaps structure on the top of the Allertal salt structure.
Der Ummendorfer Graben bildet eine Einbruchstruktur über der Salzstruktur Allertal.
Ummendorfer Graben
Crestal Graben of the Allertal salt structure
The Scheitelgraben Allertal forms a collaps structure on top of the Allertal salt structure.
Der Scheitelgraben Allertal bildet eine Einbruchstruktur im Dachbereich der Allertal Salzstruktur.
Scheitelgraben der Allertal Salzstruktur
Fallstein-Huy-Hakel Structure
The Fallstein-Huy-Hakel structure is an anticline in the Mesozoic strata of the Subhercynian Basin. It is associated with major reverse basement faults and associated flexures in the Mesozoic cover.
Der Fallstein-Huy-Hakel-Strukturzug bildet eine markante Antiklinale in der mesozoischen Schichtenfolge des Subherzynen Beckens. Diese ist an bedeutende Sockelstörungen gebunden, während in der mesozoischen Abfolge überwiegend flexurelle Falten auftreten.
Fallstein-Huy-Hakel Störungszone
Huy Fault Zone
The Huy Fault Zone forms an important basement fault of the Fallstein-Huy-Hakel structure in the Subhercynian Basin.
Die Huy Störung bildet eine markante Störungszone des des Fallstein-Huy-Hakel-Strukturzugs.
Huy-Störungszone
Fallstein Southern Border Fault
The Fallstein Soutehrn Boundary Fault forms the soutern boundary fault of the Fallstein structure.
Die Fallstein-Südrand-Störung bildet die südliche Sockelstörung des Fallstein-Huy-Hakel-Strukturzugs.
Fallstein-Südrandstörung
Fallstein Northern Border Fault
The Fallstein Northern Boundary Fault forms the northern boundary fault of the Fallstein structure.
Die Fallstein-Nordrand-Störung bildet die nördliche Sockelstörung des Fallstein-Huy-Hakel-Strukturzugs.
Fallstein-Nordrandstörung
Large Graben Fault
The Großer Graben fault zone is a E-W-trending fault zone at the state borders between Lower Saxony and Saxony-Anhalt. Although only poorly explored, the fault zone might be associated with major tectonic movements during Triassic times as proved by strongly variating thicknesses of Triassic strata.
Die Großer Graben Störungszone ist eine E-W-streichende Verwerfungszone an der Landesgrenze zwischen Niedersachsen und Sachsen-Anhalt. Obwohl nur gering untersucht, steht die Verwerfungszone möglicherweise mit bedeutenden tektonischen Bewegungen während der Trias in Verbindung, die entlang des Westrandes des Subherzynen Beckens stattfanden.
Großer Graben Störung
Oschersleben-Staßfurt Fault Zone
The Oschersleben-Staßfurt fault zone forms is a basement fault associated with the Offleben-Oschersleben-Staßfurt Salzsattel. It forms the border between the Lappwald Block in the north and the Central Subhercynian Depression.
Die Oschersleben-Staßfurt Störungszone ist eine Sockelstörung, die im Zusammenhang mit dem Offleben-Oschersleben-Staßfurt-Salzsattel steht. Sie bildet die Grenze zwischen dem Lappwaldblock im Norden und dem zentralen Subherzynen Becken.
Oschersleben-Staßfurter-Störungszone
Güsten Fault
The Güsten fault zone is one part of the Oschersleben-Staßfurt Fault zone in the central part of the Subhercynian Basin. It is associated with strong halokinetic movements und huge subsidence during Cenozoic times.
Die Güsten Störungszone bildet einen Teil der Oschersleben-Staßfurter Störungszone im zentralen Subherzynen Becken. Ihre Aktivität ist von ausgeprägten halokinetischen Bewegungen und starker Subsidenz während des Känozoikums begleitet.
Güstener Störung
Offleben Fault
The Offleben Fault Zone is one part of the Oschersleben-Staßfurt Fault zone in the westernmost Subhercynian Basin.
Die Offleben Störungszone bildet einen Teilabschnitt der Oschersleben-Staßfurter Störungszone im westlichen Subherzynen Becken.
Offlebener Störung
Paschleben Fault Zone
The Paschleben fault zone is a NW-SE-trending fault zone, which separates the Paleozoic strata of the Paschleben anticline against the Mesozoic strata of the Subhercynian Basin.
Die Paschlebener Vorsprung Störungszone ist eine NW-SE-streichende Störungszone, die die Paläozoischen Einheiten des Paschlebener Vorsprungs gegen die mesozoischen Einheiten des Subherzynen Beckens abgrenzt.
Paschlebener Störungszone
Bernburg Graben
The Bernburg Graben forms an extensional fault zone in the east of the Offleben-Oschersleben-Staßfurter Salzsattel.
Der Bernburg Graben bildet eine extensionale Störungszone im Osten des Offleben-Oschersleben-Staßfurter Salzsattels.
Bernburger Graben
Hohenerxleben Fault Zone
The Hohenerxleben fault zone is a NNE-SSW trending fault zone in the eastern Subhercynian Basin. It limits the Egelner salt structure in the southeast.
Die Hohenerxlebener Störungszone ist eine NNE-SSW streichende, Störungszone im östlichen Subherzynen Becken. Sie begrenzt den Egelner Sattel im Südosten.
Hohenerxleben-Störungszone
Hohenerxleben Fault
Athensleben Fault Zone
The Athensleben fault zone is a NNE-SSW trending fault zone that crosses the NW-SE trending main faults of the Subhercynian Basin.
Die Athenslebener Störungszone ist eine NNE-SSW streichende Störungszone, die die NW-SE-streichenden Hauptstörungen des Subherzynen Beckens quert.
Athensleben-Störung
Athensleben Fault
Gröbzig Fault Zone
The Gröbzig fault zone is a SW-NE trending fault in the northwestern part of the Halle-Wittenberg Block postulated in particular on the basis of gravity measurements.
Die Gröbziger Störung ist eine insbesondere auf der Grundlage gravimetrischer Messungen postulierte SW-NE streichende Störung im nordwestlichen Randbereich der Halle-Wittenberg-Scholle.
Gröbziger Störungszone
Gröbzig Fault
Alsleben-Gröbziger Fault Zone
The Alsleben-Gröbziger Fault Zone is part of the Gröbzig Fault Zone.
Die Alsleben-Gröbziger Störungszone bildet eine Teilstruktur der Gröbziger Störungszone.
Alsleben-Gröbzig-Störungszone
Harz Northern Border Fault
The Harz Northern Boundary Fault forms a NW-SE-trending fault zone structure that plunges to a depth of approx. 1000 m at an average dip of 60 degrees. Different offset values between 3000 m and up to 7000 m are given. The depth range is estimated to be 10-12 km, according to gravimetric indications even up to 30 km. Their first activity was probably Variscan, perhaps even pre-Variscan. Today's structur is mainly the result of multiphase post-variscan activities. During the Latest Cretaceous, the Harz Mountains were raised and their frontal thrust on their foreland was at least 2-3 km in a north-north-east direction.
Die Harz-Nordrandstörung bildet eine NW-SE-streichende und bis zu einer Teufe von ca. 1000 m mit durchschnittlich 60° oder steiler nach Süden einfallende, im Wesentlichen aus drei jeweils in das Harzpaläozoikum hineinlaufenden Teilstörungen zusammengesetzte Bruchstruktur. Als Versetzungsbetrag werden unterschiedliche Werte zwischen 3000 m und bis zu 7000 m angegeben, die Tiefenreichweite soll schätzungsweise 10-12 km, nach gravimetrischen Indikationen sogar bis 30 km betragen. Ihre Anlage erfolgte wahrscheinlich variszisch, vielleicht auch schon prävariszisch. Das heutige Strukturbild ist hauptsächlich Ergebnis mehrphasiger postvariszischer Aktivierungen. Während der späten Kreide erfolgte die Heraushebung des Harzes sowie deren Nordnordost gerichtete, mindestens 2-3 km betragende frontale Überschiebung auf ihr Vorland.
Harznordrandstörung
Harz Fault
The Flechtingen High, often referred to as the Flechtingen-Rosslau Block, forms the approx. 100 km long and 20 km wide, NW-SE trending surface outcrop of Palaeozoic rocks in central Saxony-Anhalt. In wide areas Cenozoic strata cover that basement block. The outcropping rocks were low-grade metamorphic, moderately deformed foreland sediments of the Rhenohercynian Zone as well as high-grade metamorphic and intrusive rocks in the Mid-German-Crystalline Rise. They are widely covered by Late Carboniferous to Early Permian sedimentary rocks. After the Variscan orogeny, the border faults of the Flechtingen High evolved as large dextral strike-slip faults forming the southern Elbe Zone, a crustal-scale wrench system ranging from the Bohemian Massif in the southeast to the North Sea in the northwest. It is supposed that sedimentary rocks of the Central European Basin System covered the Flechtingen High during Mesozoic times. The border faults, i.e. parts of the Elbe Zone, were probably reactivated under extension during the Jurassic to Early Cretaceous. Late Cretaceous contraction lead to the uplift of the Flechtingen High and probably affected later large-scale crustal movements as revealed by the distribution of Cenozoic strata [Stackebrandt, 1986].
Fault zones of the Flechtingen High
Der Flechtingen Höhenzug, oft als Flechtingen-Rosslau-Scholle bezeichnet, bildet einen rd. 100 km lange und 20 km breiten, NW-SE-streichenden-Oberflächenaufschluss paläozoischer Gesteine. In weiten Gebieten bedecken känozoische Schichten diesen Sockelaufbruch. Die aufgeschlossenen Gesteine ​​sind niedriggradige metamorphe Gesteine sowie mäßig deformierte Vorland-Sedimente des Rhenoherzynikums sowie hochgradige metamorphe und intrusive Gesteine ​​der Mitteldeutschen Kristallinzone. Sie sind weitgehend von Sedimentgesteinen aus spätem Karbon bis frühem Perm bedeckt. Nach der Varizischen Orogenese entwickelten sich die Randstörungen des Flechtinger Höhenzugs zu großen dextralen Scherzonen, die zusammen als südliche Elbzone beschrieben werden und ein Wrench-System im Krustenmaßstab bilden, das vom Böhmischen Massiv im Südosten bis zur Nordsee im Nordwesten reicht. Es wird vermutet, dass Sedimentgesteine ​​des mitteleuropäischen Beckensystems den Flechtinger Höhenzug während des Mesozoikums bedeckten. Die Randstörungen, d. h. Teile der Elbzone, wurden wahrscheinlich während der Jura- bis frühen Kreidezeit unter einem extensionalen Spannungsfeld als Abschiebungen reaktiviert. Einengung während der späten Kreide führte zur Anhebung des Flechtinger Höhenzugs und beeinflusste als existierende Hochlage auch spätere großräumige Krustenbewegungen, wie die Verteilung der känozoischen Sedimente zeigt [Stackebrandt, 1986].
Störungszonen des Flechtinger Höhenzugs
Störungszonen der Flechtingen-Rosslau-Scholle
Flechtingen High Southern Border Fault
The Flechtingen-Südrand fault zone delimits the Flechtingen-Rosslau Block in the north against the Subhercynian Basin in the south with comparatively small offsets.
Die Flechtingen-Südrand Störungszone begrenzt mit vergleichsweise geringen Versätzen die Flechtingen-Rosslau Scholle im Norden gegen das Subherzyne Becken im Süden.
Flechtingen-Suedrand-Störungszone
Wittenberg Fault Zone
The Wittenberg fault zone forms the eastern section of the Haldensleben fault and is thus one of the "Central German main escarpments". It borders the Flechtingen-Rosslau-Block in the south against the North German Basin in the north.
Der Wittenberg-Abbruch bildet den östlichen Abschnitt der Haldensleben Überschiebung und ist damit einer der "Mitteldeutschen Hauptabbrüche". Er begrenzt die Flechtingen-Rosslau-Scholle im Süden gegen das Norddeutsche Becken im Norden.
Wittenberg-Störungszone
Wittenberg Thrust
Abburch von Wittenberg
Haldensleben Fault Zone
The Haldensleben fault delimits the Central European Basin succession of the Calvörde Block in the north against the outcrop of Palaeozoic strata of the Flechtingen High in the south. It forms a large SW-dipping reverse fault. Uniform fault offsets only exceed 3 km in the east, where the Gardelegen fault converges with the Haldensleben fault. In its northern foreland subordinated basement faults with minor normal and reverse offsets separate Triassic to Early Jurassic strata in narrow (5 km wide) sub-basins and grabens indicating a complex pre-thrusting history. In the outer east several basement reverse faults border smaller uplifts of Palaeozoic rocks.
Die Haldensleben Überschiebung begrenzt die Scholle von Calvörde als Teil des Zentraleuropäischen Beckens im Norden gegen die paläozoischer Schichten der Flechtingen-Rosslau-Scholle im Süden. Als einer der "Mitteldeutschen Hauptabbrüche" bildet sie eine bedeutende Überschiebung mit einem Einfallen nach Südwesten. Die vergleichsweise einheitlichen Störungsversätze überschreiten im Osten selten 3 km. Hier konvergiert die Gardelegen Überschiebung mit der Haldensleben Überschiebung. Im nördlichen Vorland trennen untergeordnete Sockelstörungen mit geringfügigen Abschiebungs- und Aufschiebungsversätzen mesozoische Schichten in enge (5 km breiten) Teilbecken und Gräben, was auf eine komplexe Vorgeschichte hinweist. Im äußeren Osten grenzen mehrere Sockelstörungen an kleinere Erhebungen paläozoischer Einheiten.
Haldensleben-Störungszone
Haldensleben Thrust
Abbruch von Haldensleben
The northern part of Saxony-Anhalt (Altmark area) forms the southern rim of the Central European Basin System. It underwent continuous subsidence since Permian times. The major tectonic blocks trend either NNE-SSW or NW-SE. Hence, in earlier classifications [e.g., Katzung and Ehmke, 1993] the entire area was named ‘Altmark-Fläming Depression’. Based on more recent investigations based on extensive reflection seismic data and several hundreds of boreholes, which were combined in a homogeneous 3D geological model [Malz et al., 2020], the Altmark area can be subdivided into six major tectonic units: (1) The eastern part of the Gifhorn Trough is located in the outer northwest and forms a NNE-SSW-trending Mesozoic (trans-)tensional graben. (2) The (Eichsfeld-) Altmark Swell to the east of the Gifhorn Trough is an approximately 50 km wide NNE-SSW to NE-SW-striking structural high [Wienholz, 1964] initially emerged during the latest Permian to Triassic [Paul, 1993]. It is interpreted as the former graben shoulder of the western adjacent Gifhorn Trough [Malz et al., 2020] and is bordered by a deep crustal shear zone (Arendsee Lineament) to the east [Franke, 1990]. (3) In the northeast of the Altmark structures of similar trending direction (NNE-SSW) are associated with the Rheinsberg Trough located at the eastern border of Saxony-Anhalt. In these areas (Gifhorn Trough, Altmark Swell and Rheinsberg Trough) associated fault zones are difficult to detect due to the complex interplay of synkinematic erosion and deposition, extensive diapirism as well as crosscutting NW-SE-striking normal and reverse faults. (4) The inverted Altmark-Fläming Basin s. str. is located between the Altmark Swell and the Rheinsberg Trough. Narrow NW-SE-striking, in parts reverse reactivated normal faults and long wavelength folds, salt pillows and diapirs characterize this area. (5) The ‘Late Jurassic Altmark Swell’ borders the Altmark-Fläming Basin s. str. to the south. It forms the southern graben shoulder of the northern adjacent basin and is mostly characterized by several tens of kilometres long, Late Cretaceous short-wavelength thin-skinned folds and thrust faults. The Altmersleben-Demker Fault zone defines the border fault between the latter mentioned structural blocks.
Fault zone of the Altmark area
Störungszone des Norddeutschen Beckens
Fault Zone of the North German Basin
Störungszone der Altmark
Salzwedel Fault Zone
The regional, NW-SE-striking Salzwedel fault system crosses nearly the whole north of Saxony-Anhalt. All faults in the ‘supra-salt’ succession can be clearly correlated with corresponding basement faults. The fault zone comprises several individual fault strands (from west to east): (1) The Wustrow-Lüge-Liesten fault segment, a north-dipping major fault and with steeply south-dipping antithetic faults arranged in an anticline, shows minor normal and reverse offsets indicating a poly-phase activity. Towards the east, it becomes replaced by the (2) Lüge-Liesten-Meßdorf fault segment, which forms a steeply dipping reverse reactivated normal fault with a ‘harpoon structure’ (cf. McClay and Buchanan, 1992) in its hanging wall. Preserved syn-extensional Upper Jurassic to Lower Cretaceous strata became later uplifted and thrusted against Upper Cretaceous rocks in the footwall. In the (3) Meßdorf-Groß Schwechten fault segment the structural style changes to a south-dipping steep normal fault with relatively low offsets.
Die regionale, NW-SE-streichende Salzwedel Störungszone quert nahezu den gesamten Nordteil Sachsen-Anhalts. Ihre einzelnen Segmente werden auch nach den gequerten Salzstrukturen benannt, weshalb sich eine Unterteilung der Störungszone in einzelne Abschnitte ergibt. So werden innerhalb der Störungszone Wustrow-Lüge Liesten die Dehnungsstrukturen in der Umrahmung des Salzstockes Wustrow nach Südosten durch Einengungsstrukturen abgelöst. Die in sich gestörte NE-Flanke ist gegenüber dem SW-Flügel angehoben. Diese enthält zum Teil mächtige synkinematische Oberkreide-Sedimente. Lokal sind auf der NE-Flanke grabenbruchartige Strukturen mit Unterkreide nachgewiesen. Teilweise Salzintrusionen in die Störungszone nachgewiesen. Jüngste Bewegungen sind lokal bis ins Tertiär nachgewiesen. In Richtung Osten setzt sich die Störungszone Lüge Liesten-Meßdorf mit einem ähnlichen Strukturinventar der NE- und SW-Flanken fort. Beiderseits der Störungszone sind Senken mit kretazischen Sedimenten ausgebildet (Unterkreide im NE, Oberkreide im SW), die eine polyphase tektonische Entwicklung belegen. Die Störungszone Meßdorf-Groß Schwechten weißt eine deutliche Abweichung vom strukturellen Baustil auf. Salzintrusionen in die Störungszone sind nicht nachgewiesen. Stattdessen ist das suprasalinare Deckgebirge entlang der Störungszone deutlich in einer weitgespannten Mulde eingesunken.
Salzwedel-Störungszone
Salzwedel Fault
Wustrow-Lüge-Liesten-Meßdorf-Groß Schwechten Störungszone
Unterelbe Fault Zone
The Unterelbe fault zone as a part of the Elbe Lineament is a crustal discontinuity at the northern border of the Altmark area. In the Permian to Mesozoic cover it is represented by mild normal faulting during Jurassic-Early Cretaceous times and became reverse reactivated during Late Cretaceous basin inversion.
Unterelbe-Störungszone
Elbe Lineament
Unterelbe-Barenthin-Störung
Meseberg Fault Zone
The Meseberg fault zone is a NW-SE-trending fault zone associated with the Meseberg diapir. The activity of the fault zone is strongly associated with halokinetic movements and the formation of the Meseberg salt pillow in Late Cretaceous times.
Meseberg-Störungszone
Meseberg Fault
Meseberg-Störung
Die ungefähr 22 km lange und bis zu 5 km breite Hassel-Schwarzholz-Störungszone (Emmerlich 2017) befindet sich nördlich von Stendal in der östlichen Altmark und stellt ein NNE-SSW bis N-S streichendes Störungssystem dar, das zwischen den Salzstöcken Mahlitz im Osten und Groß Schwechten im Westen die Salzwedel-Störungszone quert. Für dieses bereits von Lapschin et al. 1972 beschriebene Störungssystem wurde im Rahmen der Modellerstellung erstmals eine Trassierung durchgeführt, um eine in sich konsistente dreidimensionale Vorstellung zum Störungsverlauf und dessen Entstehung zu entwickeln. In früheren Arbeiten (Lapschin et al. 1972) konnte diese Trassierung aufgrund der zu geringen Profildichte und einem spitzwinkligen Verlauf der Profile zu den Störungen noch nicht durchgeführt werden. Ihre Existenz wurde aber bereits in diesen Arbeiten schon auf Basis von Änderungen der Sprungtendenz und dem plötzlichen Ausklingen der die Struktur querenden und NW-SE streichenden Salzwedel-Störungszone postuliert. Bei allen Einzelbrüchen der Hassel-Schwarzholz-Störungszone handelt es sich um Abschiebungen und Grabenbrüche (Lapschin et al. 1972). Die Störungszone besteht im Modell aus zwei mehr oder weniger getrennten Systemen, einem südwestlichen Störungsabschnitt, der aus zwei Einzelbrüchen mit gegenläufigem Einfallen aufgebaut ist, und einem nordöstlichen Abschnitt mit drei Einzelbrüchen. Die Hauptstörungen beider Abschnitte bilden im Zentrum der Salzwedel-Störungszone eine Schnittlinie, an der der nordöstliche Abschnitt endet. Der südwestliche Abschnitt hingegen verläuft über nahezu die gesamte Länge der Störungszone. Die Hauptstörungen der beiden Störungsabschnitte zeigen deutlich eine Fortsetzung innerhalb der subsalinaren Einheiten, während die von ihnen begleiteten Zweigstörungen nur die Basis des Buntsandsteins versetzen. Die stratigraphisch höchsten von bruchhafter Deformation beeinflussten Einheiten sind die Horizonte der Unterkreide, deren Verbreitung sich stark an der Hassel-Schwarzholz-Störungszone orientieren. Selbiges gilt ebenfalls für die Einheiten des höheren Jura, der im weiteren Umfeld der Störungszone ausschließlich entlang dieser orientiert ist. Aufgrund dieser Verbreitung der oberjurassischen bis unterkretazischen Einheiten wird der Entstehungszeitraum der Hassel-Schwarzholz-Störungszone für den Zeitraum der Ablagerung dieser Schichten interpretiert. In Verbindung mit regionalgeologischen Betrachtungen ergibt dies eine primäre Anlage der Störungszone als Blattverschiebungssystem mit einem zum Teil deutlich abgesenkten Störungszentrum. Auch die Geometrie der Einzelstörungen sowie ihr vergleichsweise steiles Einfallen stützen diese Interpretation der Störungszone als negative Blumenstruktur (negative flower structure; vgl. Harding et al. 1985; Woodcock & Fischer 1986). Obwohl alle Einzelstörungen der Hassel-Schwarzholz-Störungszone im Hangenden durch die transgressiv überlagernden Horizonte der Oberkreide begrenzt werden, muss auch für diesen Zeitraum eine Aktivität der Störungszone im allgemein kompressiven Spannungsfeld angenommen werden. Diese Annahme begründet sich im deutlich dem Störungssystem folgenden Ausstrich der Oberkreide, die ausschließlich im Westen der Störungszone verbreitet ist. Die Tiefenreichweite dieser Bewegungen ist allerdings auf Basis der vorliegenden Daten nicht zweifelsfrei einzuschätzen, da sowohl Bewegungen an den sich ins Subsalinar fortsetzenden Störungen als auch einzig Bewegungen im Suprasalinar im Zusammenhang mit der Entstehung der umliegenden Salzstöcke möglich erscheinen.
Hassel-Schwarzholz Fault Zone
The approximately 30 km long and 1.5 km wide Hassel-Schwarzholz fault consists out of five individual normal faults with respectively low (< 50 m) fault offsets. The fault zone retraces the axis of a NNE-SSW trending sub-basin located directly between the Groß Schwechten and Mahlitz diapirs. Due to its spatial relation to the Late Jurassic-Early Cretaceous sub-basin we interpret that transtensional/extensional faulting started synchronously. Furthermore, the fault zone's location coinciding with the eastern outline of Late Cretaceous strata probably suggests a Late Cretaceous transpressional/compressional overprint.
Hassel-Schwarzholz-Störungszone
Hassel-Schwarzholz Fault
Hassel-Schwarzholz-Störung
Seehausen Fault Zone
The Seehausen fault zone is a NW-SE-trending extensional fault zone in the Permian to Mesozoic strata of the northeastern Altmark area.
Seehausen-Störungszone
Seehausen Fault
Seehausen-Störung
Groß Schwechten Fault Zone
The Groß Schwechten fault zone consists of three normal faults located on the outer limbs of the associated Groß Schwechten salt pillow. All faults dip towards the centre of the diapir. A relatively uniform layering of Triassic to lower Middle Jurassic strata suggests that deformation and vertical movements started in Late Jurassic-Early Cretaceous times at the earliest. The regional Late Cretaceous unconformity sealing the entire fault zone marks the end of deformation.
Die Störungszone Groß Schwechten bildet eine NNE-SSW streichende Grabenstruktur in der östlichen Altmark. Ihre Namensgebung beruht auf dem sich in ihrem Grabeninneren befindenden Salzstock Groß Schwechten (Emmerlich 2017). Die ungefähr 2,5 km breite und bis zu 17 km lange Störungszone besteht aus einer östlichen Hauptstörung und einer westlichen antithetischen Zweigstörung. Bei beiden Störungen handelt es sich um Abschiebungen, die durch die Transgression der Oberkreide nach oben hin begrenzt sind. Eine Fortsetzung der Störungen im Subsalinar deutet sich auf vielen reflexionsseismischen Profilen an und ist als wahrscheinlich anzunehmen. Die Ausbildung der Störungszone wird für den Zeitraum Oberjura/Unterkreide angenommen, und steht in engem Zusammenhang mit der Ausbildung eines Salzkissens unter dem heutigen Salzstock Groß Schwechten. Aus regionalgeologischen Betrachtungen zur Hauptspannungsrichtung während des Zeitraums Oberjura/Unterkreide (Franzke et al. 2007; Navabpour et al. 2017; Sippel et al. 2009) handelt es sich bei der Störungszone, wie auch bei den anderen Randelementen des Rheinsberg-Trogs, um transtensionale Strukturen, die einen deutlichen Blattverschiebungsversatz aufweisen sollten.
Groß Schwechten-Störungszone
Groß Schwechten Fault
Schrampe Fault Zone
The Schrampe fault zone is a NW-SE-trending fault zone in the Mesozoic cover in the NW of the Arendsee diapir. It is elongated from the state border between Lower Saxony in the west to the Arendsee diapir in the east.
Schrampe-Störungszone
Schrampe Fault
Schrampe-Störung
Crestal Graben of the Peckensen diapir
The Scheitelgraben Peckensen forms a collaps structure on top of the Peckensen diapir.
Der Scheitelgraben Peckensen bildet eine Einbruchstruktur im Dachbereich Salzstocks Peckensen.
Scheitelgraben des Salzstocks Peckensen
Parsau Fault Zone
The Parsau fault zone forms a complex, small-scale fault zone in the western Altmark. Due to the intersection of several strike directions, this fault zone is characterized by steeply dipping layers and small-scale changing offsets.
Die Parsau Störungszone bildet eine komplexe, kleinräumige Störungszone in der westlichen Altmark. Aufgrund der Kreuzung mehrerer Streichrichtungen ist diese Störungszone durch steil einfallende Schichten und kleinräumig wechselnde Versätze charakterisiert.
Parsau-Störungszone
Parsau Fault
Parsau-Störung
Tarnefitz Fault Zone
The Tarnefitz fault zone forms a Cenozoic fault zone in the southern Altmark. It is only found in the Cenozoic sediments.
Die Tarnefitz Störungszone bildet eine känozoische Störungszone in der südlichen Altmark. Sie ist ausschließlich in den känozoischen Sedimenten nachgewiesen.
Tarnefitz-Störungszone
Arendsee Fault Zone
The Arendsee fault zone, locally named Arendsee-Lüge-Liesten or Wittenberge-Arendsee fault, is located above an 80 km long crustal structure, the Arendsee Lineament respectively (Franke, 1990). Major faults steeply (c. 70°) dip towards the west and form narrow grabens. Generally fault throws are low, locally cease and rarely exceed 200 m. The Arendsee-Lüge-Liesten and the Wittenberge-Arendsee faults form narrow northeast-dipping grabens in ‘supra-salt’ strata located above a southeast-dipping ‘sub-salt’ crustal fault zone, the Arendsee Lineament respectively.
Die Arendsee Störungszone, die lokal entsprechend ihrer Einzelsegmente auch als Arendsee-Lüge Liesten oder Wittenberge-Arendsee Störung bezeichnet wird, befindet sich über einer 80 km langen tiefreichenden, krustalen Bruchstruktur, dem Arendsee-Lineament (Franke, 1990). Die Hauptstörungen fallen steil (ca. 70°) nach Westen ein und bilden zusammen mit ihren antithetischen Störungen schmale Gräben. Im Allgemeinen sind die Versatzbeträge gering, nehmen stellenweise aber auf kurze Distanz stark ab und überschreiten selten 200 m. Die Arendsee-Lüge Liesten und Wittenberge-Arendsee Störungen bilden schmale, nach Nordosten abgesenkte Gräben innerhalb der suprasalinaren Einheiten, die sich über einer nach Südosten einfallenden subsalinaren Sockelabschiebung, dem Arendsee-Lineament, befinden.
Arendsee-Störungszone
Arendsee Lineament
Crestal Graben of the Arendsee diapir
The Scheitelgraben Arendsee forms a collaps structure on top of the Arendsee diapir.
Der Scheitelgraben Arendsee bildet eine Einbruchstruktur im Dachbereich des Arendsee Salzstocks.
Scheitelgraben des Salzstocks Arendsee
Scheitelgraben Arendsee
Jübar Fault Zone
The Jübar fault zone forms a complex, small-scale fault zone in the western Altmark. Due to the intersection of several strike directions, this fault zone is characterized by steeply dipping layers and small-scale changing offsets.
Die Jübar Störungszone bildet eine komplexe, kleinräumige Störungszone in der westlichen Altmark. Aufgrund der Kreuzung mehrerer Streichrichtungen ist diese Störungszone durch steil einfallende Schichten und kleinräumig wechselnde Versätze charakterisiert.
Jübar-Störungszone
Jübar Fault
Jübar-Störung
Neuferchau Graben
The Neuferchau fault zone forms a Cenozoic fault zone in the southwestern Altmark. It is only found in the Cenozoic sediments.
Die Neuferchauer Störungszone bildet eine känozoische Störungszone in der südwestlichen Altmark. Sie ist ausschließlich in den känozoischen Sedimenten nachgewiesen.
Neuferchauer Graben
Elster Fault Zone
The Elster fault zone forms a subordinate fault zone in the direct foreland of the Gardelegen thrust.
Die Elster Störungszone bildet eine untergeordnete Störungszone im direkten Vorland der Gardelegen Überschiebung.
Elster-Störungszone
Elster Fault
Zahna Fault Zone
The Zahna fault zone forms a subordinate fault zone in the direct foreland of the Gardelegen thrust.
Die Zahna Störungszone bildet eine untergeordnete Störungszone im direkten Vorland der Gardelegen Überschiebung.
Zahna-Störungszone
Zahna Fault
Schönewalde Fault Zone
The Schönewalde fault zone forms a subordinate fault zone in the direct foreland of the Gardelegen thrust.
Die Schönewalde Störungszone bildet eine untergeordnete Störungszone im direkten Vorland der Gardelegen Überschiebung.
Schönewalde-Störungszone
Schönewalde Fault
Schönewalde-Störung
Schweinitz Fault Zone
The Schweinitz fault zone forms a subordinate fault zone in the direct foreland of the Gardelegen thrust.
Die Schweinitz Störungszone bildet eine untergeordnete Störungszone im direkten Vorland der Gardelegen Überschiebung.
Schweinitz-Störungszone
Schweinitz Fault
Schweinitz-Störung
Schollene Fault Zone
The Schollene fault zone is a major basement fault in the northestern Altmark area.
Die Schollene Störungszone bildet eine bedeutende Sockelstörung in der nordöstlichen Altmark.
Schollene-Störungszone
Schollene Fault
Schollene-Störung
Schorstedt Fault Zone
The Schorstedt fault zone is a subordinated basement fault in the northern Altmark area, which is probably associated with Permian and Triassic extension relating to the formation of the Rheinsberg Trough.
Die Schorstedt Störungszone bildet eine untergeordnete Störungszone in der nördlichen Altmark. Als extensionale Störungszone in den Permo-Triassischen Einheiten ausgebildet, steht ihre Bildung mit der Entstehung des Rheinsberg Troges in Zusammenhang.
Schorstedt-Störungszone
Schorstedt Fault
Schorstedt-Störung
Kleinau Fault Zone
The Kleinau fault zone is a subordinated basement fault south of the Arendsee diapir.
Die Kleinau Störungszone bildet eine untergeordnete Sockelstörung im Süden des Salzstocks Arendsee.
Kleinau-Störungszone
Kleinau Fault
Kleinau-Störung
Mahlitz Fault Zone
The Mahlitz fault, which crosses the Mahlitz diapir, forms a single east-dipping normal fault with vertical offsets not exceeding 100 m. Indications for the onset of fault activity are scarce due to a Late Jurassic to Late Cretaceous hiatus. Nevertheless, from adjacent structures a synchronous onset of transtensional/extensional faulting and salt migration into the Mahlitz salt pillow during Late Jurassic/Early Cretaceous times must be supposed.
Die Mahlitz-Störung, eine den Salzstock Mahlitz in NNE-SSW-Richtung querende und nach diesem benannte Störung (Emmerlich 2017), befindet sich in der östlichen Altmark und versetzt entlang ihrer nach Osten einfallenden Störungsfläche die Modellhorizonte des Zechsteins bis zur Oberkreide. Basierend auf den Ergebnissen der reflexionsseismischen Messungen (Muraschew et al. 1972) ist von einer Sprunghöhe zwischen 50 und 100 m bei einem abschiebenden bis transtensionalen Versatzsinn auszugehen. Diese vergleichsweise geringe Sprunghöhe erschwert die Einschätzung der Begrenzung der Störung im Hangenden. Diese kann sowohl durch ein allmähliches Abklingen der Sprunghöhe aber auch als abruptes Ende der Deformation in prätertiärer Zeit angesehen werden (Küstermann 1972). Im Modell wurde deshalb davon ausgegangen, dass die Störung ausschließlich prätertiäres Alter aufweist und die Transgression des Oberpaläozäns die Störung im Hangenden begrenzt.
Mahlitz-Störungszone
Mahlitz Fault
Mahlitz-Störung
Kakerbeck-Mahlpfuhl Fault Zone
The Kakerbeck-Mahlpfuhl fault zone is a narrow, NW-SE-striking structure. It forms a large, faulted NE-vergent anticline in the west. Fault offsets do not exceed 500 m, but a huge structural heave of the hanging wall is associated with an up to one kilometre thick salt core. Thickness variations of Early Jurassic strata infer that contractional deformation overprinted a complex pre-thrusting configuration with inherited normal faults and differentially subsided blocks. Towards the east offsets decrease over short distances. Here, the fault zone is replaced by a narrow salt-cored anticline (detachment fold) with Late Cretaceous synkinematic strata in the north and south.
Die Kakerbek-Mahlpfuhl Störungszone ist eine kurzwellige, NW-SE-streichende Struktur. Im Westen bildet sie eine NE-vergente Antiklinale. Störungsversätze sind vergleichsweise gering und übersteigen nur selten 500 m. Dennoch ist die SW-Flanke der Struktur hier aufgrund von deutlicher Salzakkumulation im Kern der Antiklinale bedeutend gegenüber der NE-Flanke gehoben. Mächtigkeitsvariationen innerhalb des Jura deuten darauf hin, dass die deutliche einengende Deformation während der späten Kreide eine sehr komplexe Konfiguration mit vererbten Abschiebungen und unterschiedlich stark abgesenkten Blöcken überprägte. In Richtung Osten nehmen die Versatzbeträge der Einzelstörungen kontinuierlich ab und die Störungszone wird durch eine enge Antiklinale mit mächtigem Salzkern (Detachment-Falte) vertreten, die durch mächtige spätkretazische Sedimente im Norden und Süden begleitet wird.
Kakerbeck-Mahlpfuhl-Störungszone
Burg-Reuden Fault Zone
The Burg-Reuden fault consists of the western (‘Burg’) part, where a single reverse fault exists in the outer crest of a salt-cored anticline in its hanging wall. Here, similar fault offsets (300 m) in the cover and the basement exist. In the eastern (‘Reuden’) part relatively high fault offsets (1 km) exist at the intersection with the Brehm fault indicating a significant amount of displacement transfer from that structure.
Die Burg-Reuden Störungszone besteht aus dem westlichen Teil („Burg“), in dem eine einzige Aufschiebung im äußeren Bogen einer Detachment Falte vorliegt. Hier bestehen ähnliche Versatzbeträge (300 m) im Sockel wie auch im Deckgebirge. Im östlichen Teil („Reuden“) sind im Kreuzungsbereich mit der Brehm Störungszone relativ hohe Versätze (1 km) auszumachen, was auf einen erheblichen Versatztransfer zwischen diesen Strukturen hinweist.
Burg-Reuden-Störungszone
Burg-Reuden Fault
Ahlum Fault Zone
The Ahlum fault zone forms the western elongation of the Gardelegen fault in map view. It is bounded by up to 2.5 km thick Late Cretaceous strata in the north and south. The fault zone is <1.5 km wide and reverse offsets (up to 1.5 km) are restricted to the Mesozoic cover. Hence, we interpret the Ahlum fault to represent a thin-skinned reverse fault, which thus must be kinematically linked to thick-skinned thrusting farther south; i.e., at the western Gardelegen fault.
Die Ahlum Störungszone erstreckt sich zwischen dem Salzstock Ristedt und dem Südende des Salzstocks Peckensen. Sie bildet die westliche Verlängerung der Gardelegen Störung im Kartenbild. Sie ist asymmetrisch aufgebaut und sehr deutlich kompressiv überprägt. Sie weißt eine intensive bruchtektonische Zerlegung der Südflanke und des Strukturtops auf. Teilweise überkippte Lagerung der Schichtenfolge belegt zusätzlich die kompressive Überprägung. Charakteristisch für die Ahlum Störungszone ist ihre vergleichsweise enge Ausbildung im Vergleich zu ihren beiderseits vorhandenen bis zu 1,5 km mächtigen Randsenken mit spätkretazischen Sedimenten.
Ahlum-Störungszone
Ahlum Fault
Crestal Graben of the Jahrstedt diapir
The Scheitelgraben Jahrstedt forms a collaps structure on top of the Jahrstedt diapir.
Der Scheitelgraben Jahrstedt bildet eine Einbruchstruktur im Dachbereich des Jahrstedt Salzstocks.
Scheitelgraben des Salzstocks Jahrstedt
Crestal Graben of the Apenburg and Poppau diapirs
The Scheitelgraben Apenburg-Poppau forms a collaps structure on top of the Apenburg and Poppau diapirs.
Der Scheitelgraben Apenburg-Poppau bildet eine Einbruchstruktur im Dachbereich der Salzstöcke Apendburg und Poppau.
Scheitelgraben der Salzstöcke Apenburg und Poppau
Uelzen Fault Zone
The Uelzen Lineament forms an inverted halfgraben with a listric, north-dipping normal fault flattening in the mechanically weak strata of the Zechstein group and the Upper Buntsandstein subgroup. Due to prior intense E-W extension along bedding parallel normal faults these weak strata are super-imposed. Hence, flattening of the listric Uelzen normal fault may was associated with the reactivation of a pre-existing shear zone within the basal detachment. Antithetic normal faults of the Uelzen Lineament lead to subordinate syntectonic basins with steeply dipping (up to 45°) Late Jurassic strata. Late Cretaceous syn-contractional deposits in the footwall and in the farther hanging wall prove a contractional overprint and retrace the typical distribution of synkinematic strata adjacent to inverted halfgrabens with reactivated listric normal faults (Buchanan and McClay, 1991).
Das Uelzen-Linieament bildet einen invertierten Halbgraben mit einer listrischen, nach Norden einfallenden Hauptstörung. Diese zeigt eine Verflachung in den Salinaren des Zechsteins und Oberen Buntsandsteins. Aufgrund der vorherigen intensiven E-W-Ausdehnung entlang schichtparalleler Abschiebungen liegen diese mechanisch weichen Schichten in störungsbedingt direkt übereinander. Daher kann eine Abflachung der listrischen Uelzen-Hauptabschiebung während der spätjurassischen Extension mit der Reaktivierung einer bereits vorhandenen, triassischen Scherzone innerhalb des Zechsteins verbunden sein. Antithetische Abschiebungen des Uelzen-Linieaments führen zu untergeordneten syntektonischen Sedimentbecken mit steil abfallenden (bis zu 45 °) spätjurassischen Sedimenten. Spätkretazische syn-kontraktionale Ablagerungen im Liegenden und Hangenden der Hauptstörung belegen die spätkretazische Inversion und zeichnen die typische Verteilung von synkinematischen Schichten neben invertierten Halbgrabenen mit reaktivierten listrischen Hauptabschiebungen nach.
Uelzen-Lineament
Uelzen Lineament
Bierstedt Fault Zone
The Bierstedt fault forms a normal fault in the east of the Peckensen diapir on top of the Altmark Swell. It forms the easternmost expression of the Uelzen Lineament, where it crosses the Peckensen diapir.
Die Bierstedt Störung bildet eine Abschiebungszone im Osten des Salzstocks Peckensen im Top-Bereich der Altmark Schwelle. Sie bildet das östliche Ende des Uelzen-Lineaments, wo dieses den Salzstock Peckensen kreuzt.
Bierstedt-Störungszone
Bierstedt Fault
Bierstedt-Störung
Crestal Graben of the Ristedt diapir
The Scheitelgraben Ristedt forms a collaps structure on top of the Ristedt diapir.
Der Scheitelgraben Ristedt bildet eine Einbruchstruktur im Dachbereich des Ristedt Salzstocks.
Scheitelgraben des Salzstocks Ristedt
Altmersleben-Demker Fault Zone
The Altmersleben-Demker fault zone forms an 80 km long structure, which roughly coincides with the southern distribution outline of Late Jurassic and Lower Cretaceous strata. The north-dipping steep major fault and several antithetic faults form a narrow graben structure located in the crest of an anticline. In the west, the fault zone abruptly starts with a vertical displacement of 500 m, large fault offsets and a south-vergent anticline. To the east, fault offsets decrease over a short distance and the entire structure is only mildly folded and faulted. Farther east, large normal offsets in Triassic strata are detectable, while the Late Jurassic-Early Cretaceous basin fill was uplifted, folded and faulted with reverse sense.
Die Störungszone Altmersleben-Demker bildet eine NW-SE-streichende Störungszone im Norden Sachsen-Anhalts. In ihrem Nordwesten ist sie als weitgespannte, störungsgebundene, in Richtung Südwesten überschobene Antiklinale mit Scheitelstörungen ausgebildet. In Richtung Osten wird der Bau der Störungszone komplizierter. Entlang der Störungszone ist das Salz unterschiedlich hoch aufgedrungen und bildet stellenweise diapirartige Körper (Altmersleben, Berkau) aus. In Richtung Osten zeigt die Störungsfläche innerhalb der post-salinaren Einheiten ein deutlich steileres Einfallen. Die deutlich in Richtung Nordosten einfallenden Hauptstörung zeigt anhand der sie begrenzenden Schichtenfolge und deren Mächtigkeit deutliche Anzeichen für eine spätjurassisch/frühkretazische extensionale Aktivität und daran anschließende spätkretazische Phase der Einengung (Inversion des nördlich angrenzenden Grabens).
Altmersleben-Demker-Störungszone
Genthin-Störung
Crestal Graben of the Lüge-Liesten and Meßdorf diapirs
The Scheitelgraben Lüge-Liesten-Meßdorf forms a collaps structure on top of the Lüge-Liesten and Meßdorf diapirs and the salt-related faults of the Salzwedel fault zone.
Der Scheitelgraben Lüge-Liesten-Meßdorf bildet eine Einbruchstruktur im Dachbereich der Salzstöcke Lüge-Liesten und Meßdorf sowie der diese verbindenden Salzwedel Störungszone.
Scheitelgraben der Salzstöcke Lüge-Liesten und Meßdorf
Rockenthin-Peckensen-Gladdenstedt Fault Zone
The Rockenthin-Peckensen-Gladdenstedt fault zone striking NNE-SSW is a major fault zone associated with a highly complex fault system at the outer eastern border of the Gifhorn Trough. The major fault of this system forms a mildly westward-dipping, bedding-parallel normal fault with associated antithetic normal faults in its hanging wall. In parts subordinated extensional detachments and duplexes occur between the Triassic salt horizons (Upper Buntsandstein and Middle Muschelkalk detachments) and the Zechstein evaporites. Thickness distribution and a local hiatus between Buntsandstein and Upper Keuper (Arnstadt and Exter Fm.) strata suggest that major faulting occurred due to E-W-directed extension during Late Triassic (Karnian) times. During Late Jurassic to Early Cretaceous times the fault zone became reactivated under extension/transtension as inferred by the onset of diapirism at the Peckensen salt dome. In parts subsequent contraction during Late Cretaceous times is inferred.
Bei der NE-SW-streichenden Störungszone Rockenthin-Peckensen-Gladdenstedt handelt es sich um eine komplexe Störungszone, die im Zusammenhang mit dem Störungssystem am Ostrand des Gifhorn-Trogs steht. Über einem Salzkern angelegt, ist der südöstliche Bereich deutlich gegenüber dem Nordwesten gehoben. Dies veranlasste Benox et al. (1997) zu der Deutung, dass es sich um eine nach Nordwesten gerichtete Aufschiebung handelt. Neuere Interpretationen im Bereich der Rockenthin-Peckensen-Gladdenstedt Störungszone (Malz et al., 2020) weise dagegen darauf hin, dass die Störungszone ein komplexes System aus ursprünglich altkimmerisch (Karnium) angelegten, flachen Abschiebungen bildet, welches sowohl während der spätjurassisch-frühkretazischen Dehnung transpressiv als auch während der spätkretazischen Einengung transpressiv überprägt wurde. Dies ist sowohl durch unterschiedlich tiefreichende Diskordanzen innerhalb des Mesozoikums, die Verbreitung und Mächtigkeit der Sedimente als auch durch das Einsetzen des Diapirsmus am Salzstock Peckensen belegt. Die Versatzbeträge der Störungszone klingen sowohl von Norden als auch von Süden zum Salzstock Peckensen hin aus. Dennoch lässt sich die Existenz der Störungszone unter dessen Salzüberhängen aufgrund von unterschiedlichen strukturellen Niveaus im Osten und Westen des Salzstocks als gesichert annehmen.
Rockenthin-Peckensen-Gladdenstedt Störungszone
Peckensen-Störung
Brehm Fault Zone
The Brehm fault forms the 30 km long, along-strike continuation of the Gardelegen fault in the Mesozoic cover. Single reverse faults are arranged in a 4 km wide anticline bordered by synclines filled with Late Cretaceous strata. To the east the Brehm fault converges towards the Burg-Reuden fault farther south.
Die Brehm Störungszone bildet die 30 km lange, östliche Fortsetzung der Gardelegen-Verwerfung in den mesozoischen Sedimenten. Lokal sind Aufschiebungen in einer bis zu 4 km breiten Antiklinale angeordnet, die von Synklinalen im Norden und Süden begrenzt wird. Diese sind mit Sedimenten spätkretazischen Alters gefüllt. Im Osten konvergiert die Brehm Störungszone mit der Burg-Reuden Störungszone.
Brehm-Störungszone
Brehm Fault
Gerstedt Fault Zone
The Gerstedt fault forms an E-W-striking fault zone, with a northdipping major reverse fault and minor antithetic back thrusts or reverse reactivated normal faults. Syn-extensional strata in the hanging wall indicate Early Cretaceous halfgraben formation and (Late Cretaceous) inversion. Fault offsets are relatively high (up to 1.5 km), which can be seen by Middle to Late Triassic strata located next to Upper Cretaceous rocks. Further subhorizontal thrusts in the footwall range some hundred meters far to the south (i.e., below the Peckensen diapir) and indicate a distinct amount of yet unrecognized thin-skinned thrusting.
Die Störungszone Gerstedt bildet eine E-W-streichende Störungszone, die im Westen zwischen den Salzstöcken Wustrow und Peckensen beginnt und sich in Richtung Osten hin zum Salzstock Lüge-Liesten erstreckt. Die zum Teil stark gestörte Nordflanke ist gegenüber der Südflanke deutlich überschoben. Zum Teil setzen sich diese Überschiebungen bis in den Fußbereich des Salzstocks Peckensen als flache Überschiebungen in Form von zum Teil mehreren Hundertermeter langen Schuppen fort. Vielfache Bohrungen, die in geringen Teufen zum Teil mächtiges Salz antrafen, deuten auf einen deutlichen Salzeinschub in die Störungszone hin, weshalb diese oftmals als Salzstock gedeutet wurde. Aufgrund der erbohrten stratigraphischen Abfolge und widersprechender geophysikalischer, hauptsächlich reflexionsseismischer Belege sind diese zum Teil mächtigen Salzvorkommen allerdings als lokale Verdickungen triassischer Salinare (Röt und Muschelkalk) zu deuten. Das Vorkommen mächtiger Unterkreidesedimente auf der Nordflanke, die auf der Südflanke fehlen und durch spätkretazische Sedimente vertreten werden, deuten auf eine deutliche Vorprägung der spätkretazischen Einungsstruktur durch frühkretazische Abschiebungen hin.
Gerstedt-Störungszone
Gerstedt Fault
Strukturzug Groß Gerstedt
Zerben Fault Zone
The Zerben fault (the eastern elongation of the Kakerbek-Mahlpfuhl fault zone) forms a large, faulted NE-vergent anticline in the west. Fault offsets do not exceed 500 m, but a huge structural heave of the hanging wall is associated with an up to one kilometre thick salt-cored anticline (detachment fold) with Late Cretaceous synkinematic strata in the north and south.
Die Zerben Störungszone (östliche Verlängerung der Kakerbek-Mahlpfuhl Störungszone) bildet eine große, gestörte nordost-vergente Antiklinale im Westen. Störungsversätze übersteigen nirgendwo 500 m, aber die Hebungsbeträge der Schichtenfolge im Hangenden deuten auf eine bedeutend größere Einengung hin, die mit einer deutlichen Akkumulation von Zechstein Salzen im Kern einer bis zu einem Kilometer mächtigen Detachment Falte und mächtigen spätkretazischen Sedimenten im Norden und Süden einhergehen.
Zerben-Störungszone
Zerben Fault
Kerkau Fault Zone
The Kerkau fault zone is a subordinated basement fault south of the Arendsee diapir.
Die Kerkau Störungszone bildet eine untergeordnete Sockelstörung im Süden des Salzstocks Arendsee.
Kerkau-Störungszone
Kerkau Fault
Kerkau-Störung
Schieben Fault Zone
The Schieben fault zone forms a small-scale and subordinate fault zone in the border area of the Altmark threshold and the Altmark-Fläming basin.
Die Schieben Störungszone bildet eine kleinräumige und untergeordnete Störungszone im Grenzbereich der Altmark Schwelle und des Altmark-Fläming-Beckens.
Schieben-Störungszone
Schieben Fault
Schieben-Störung
Kuhfelde Fault Zone
The Kuhfelde fault zone forms a small-scale and subordinate fault zone in the border area of the Altmark threshold and the Altmark-Fläming basin.
Die Kuhfelde Störungszone bildet eine kleinräumige und untergeordnete Störungszone im Grenzbereich der Altmark Schwelle und des Altmark-Fläming-Beckens.
Kuhfelde-Störungszone
Kuhfelde Fault
Kuhfelde-Störung
Fleetmark Fault Zone
The Fleetmark Fault Zone is a minor fault zone in northern Saxony-Anhalt.
Die Fleetmark-Verwerfungszone ist eine kleinere Verwerfungszone in Nordsachsen-Anhalt.
Fleetmark Störungszone
Gifhorn Trough Eastern Border Fault Zone
The Gifhorn Trough Eastern Border Fault is a flat, detachment-related normal fault in the westernmost Altmark area. With large normal offsets of up to 7 km this NNE-SSW-trending fault system separates the Altmark Swell in the east towards the Gifhorn Trough in the west.
Die Ostrandstörung des Gifhorn Trogs ist charakterisiert durch eine Vielzahl flacher, abgescherter Abschiebungen mit großen Versätzen von bis zu 7 km. Diese NNE-SSW-streichende Störungszone trennt die Altmark Schwelle im Osten gegen den Gifhorn Trog im Westen.
Gifhorn Trog-Ostrand-Störungssystem
Crestal Graben of Bonese and Waddekath diapirs
The Scheitelgraben Bonese-Waddekath forms a collaps structure on top of the Bonese and Waddekath diapirs.
Der Scheitelgraben Bonese-Waddekath bildet eine Einbruchstruktur im Dachbereich der Salzstöcke Bonese und Waddekath.
Scheitelgraben der Salzstöcke Bonese und Waddekath
Diesdorf Fault Zone
The Diesdorf fault as well as minor faults near the Bonese and Waddekath diapirs are NNE-SSW-striking structures associated with a highly complex fault system at the outer eastern border of the Gifhorn Trough. The major fault of this system forms a mildly westward-dipping, bedding-parallel normal fault with associated antithetic normal faults in its hanging wall. In parts subordinated extensional detachments and duplexes occur between the Triassic salt horizons (Upper Buntsandstein and Middle Muschelkalk detachments) and the Zechstein evaporites. Thickness distribution (e.g., up to 1.5 km Middle Keuper strata in the vicinity of the Bonese/Waddekath diapirs) and a local hiatus between Buntsandstein and Upper Keuper (Arnstadt and Exter Fm.) strata suggest that major faulting occurred due to E-W-directed extension during Late Triassic (Karnian) times. During the Late Jurassic in parts this system became reactivated under extension/transtension as inferred by corresponding strata only preserved west of the Diesdorf fault.
Die Diesdorfer Störungszone (Benox et al. 1997) bildet eine N-S streichende Störungszone, die sich in etwa in der Mitte zwischen den Salzstöcken Peckensen und Bonese auf einer Länge von ca. 7 km bis zur Landesgrenze zu Niedersachen erstreckt. Diese Störungszone, auf die bereits durch Arndt et al. (1978) hingewiesen wurde und die dort als zur Randsenke des Salzstocks Peckensen hin einfallende Störung gedeutet wurde, stellt auf Basis neuerer reflexionsseismischer Messungen (Hesche et al. 1985) einen im Intervall des Jura bis zu 1,5 km breiten Grabenbruch dar, dessen Grabeninneres durch mehrere Einzelbrüche gegliedert ist. Diese Einzelbrüche weisen allesamt ein Einfallen nach Osten hin auf. Im hier beschriebenen 3D-Modell ist die Störungszone durch zwei Einzelstörungen abgebildet, eine östliche und nach Westen einfallende Hauptabschiebung sowie deren antithetische Zweigstörung. Die Schnittlinie beider Störungen befindet sich innerhalb des Keuper-Intervalls, so dass die tieferen triassischen Einheiten einzig durch die Hauptabschiebung beeinflusst sind. In Richtung Norden verliert die Störungszone allmählich an Versatz und endet sie ungefähr 1 km südlich der Landesgrenze zu Niedersachsen. Ihre Südbegrenzung bilden die Störungen des Uelzener Lineaments zwischen den Salzstöcken Bonese und Peckensen. Auffällig an dieser Störungszone ist ihre Position relativ zu den sie umgebenden Störungszonen. So bildet sie im Bereich der westlichen Altmark ein relativ selten beobachtetes Lineament, das nur eng begrenzt auftritt und weder im Norden noch im Süden eine Fortsetzung oder Entsprechung findet. Hierbei weist die Störung relativ zur für diese Region strukturprägenden „Pauline-Störung“ eine prominente Position auf. Die Diesdorfer Störungszone befindet sich exakt über der Position der für die „Pauline-Störung“ beschriebenen Rampe im unteren und mittleren Buntsandstein. Diese Position liefert Hinweise auf ihre mögliche Entstehung und eventuelle genetische Zusammenhänge, weshalb die Diesdorfer Störung als Begleiterscheinung der „Pauline-Störung“ angesehen werden muss, die sich am Übergang einer Flachbahn zur Rampe gebildet hat. Allerdings ist aufgrund der enthaltenen stratigraphischen Abfolge in diesem Bereich keine exakte Aussage zur zeitlichen Entwicklung zu treffen. Ablagerungen des Mittleren Keupers fehlen in diesem Bereich fast vollständig und die Schichtenfolge wird durch die Diskordanz des Steinmergelkeupers nach oben begrenzt. Dennoch lässt sich für die Diesdorfer Störungszone im Gegensatz zur „Pauline-Störung“ eine deutliche Aktivität während des Jura annehmen. Die Diesdorfer Störungszone wird deshalb aufgrund ihrer Position und der zeitlichen Einschränkungen bezüglich ihrer Entwicklung als eine durch die Randstörungen des Gifhorn-Trogs strukturell vorgeprägte Störung angesehen, die maßgeblich während des späten Jura tektonisch wirksam wurde und vielfach eine Reaktivierung bis ins Tertiär erfuhr.
Diesdorf-Störungszone
Diesdorf Fault
Jahrstedt-Ristedt-Poppau-Apenburg Fault Zone
The Jahrstedt-Ristedt-Poppau-Apenburg fault zone forms a regional fault zone of the Arendsee lineament. It extends from the Lüge-Liesten diapir in the north to the Jahrstedt diapir in the south. In general, the fault zone forms a westward dipping normal fault that can be traced through the entire Mesozoic and large parts of the Cenozoic strata.
Die Jahrstedt-Ristedt-Poppau-Apenburg Störungszone bildet eine regionale Störungszone des Arendsee-Lineaments. Sie erstreckt sich vom Salzstock Lüge-Liesten im Norden bis südlich des Salzstocks Jahrstedt. Generell bildet die Störungszone eine nach Westen einfallende Abschiebung, die sich durch die gesamte mesozoische und weite Teile känozoische Schichtenfolge hindurch verfolgen lässt.
Jahrstedt-Ristedt-Poppau-Apenburg-Störungszone
Fault zones of the Thuringian Basin
NW-SE- and subordinated NNE-SSW-striking fault zones, long-wavelength folds and local Cenozoic depressions characterize the southern part of Saxony-Anhalt, which belong to larger structure referred to the Thuringian Basin. The deep Palaeozoic structure comprises NE-SW-trending faults and folds of the Rhenohercynian Zone in the west and the Saxothuringian Zone in the southeast of the former Rheic Suture Zone (Mid-German Crystalline Rise). This crystalline to low-grade metamorphic basement is segmented by the NE-SW-striking, Permocarboniferous ‘Saale Depression’ [Kuhnert, 1995; Schneider et al., 2005]. Faults and structures of Mesozoic age dominantly strike NW-SE and subdivide the northeastern Thuringian Syncline. In parts these faults border small basement uplifts (e.g., the Kyffhäuser Mountains, the Bottendorf High and the Hornburg Anticline) or separate local depressions in the Mesozoic cover against each other [Katzung and Ehmke, 1993]. Thereby, faults of the Thuringian Syncline typically show low normal or reverse offsets, which is probably due to reverse reactivation of former normal faults [cf. Kley, 2013; Malz, 2014 and references therein].
NW-SE- und untergeordnete NNE-SSW-streichende Störungszonen, langwellige Falten und lokale känozoische Senken charakterisieren den südlichen Teil von Sachsen-Anhalt, der zu einer größeren Struktur gehört, dem Thüringer Becken. Die tiefe paläozoische Struktur umfasst NE-SW-streichende Störungen und Falten der Rhenoherzynischen Zone im Westen und der Saxothuringischen Zone im Südosten der ehemaligen Rheischen Sutur (repräsentiert durch die Mitteldeutsche Kristallinzone). Dieser kristalline bis niedriggradig metamorphe Sockel wird durch die NE-SW-streichende, permokarbone „Saale-Senke“ segmentiert [Kuhnert, 1995; Schneider et al., 2005]. Störungen und Strukturen des Mesozoikums streichen vorwiegend NW-SE und unterteilen die nordöstliche Thüringer Mulde in schmale "Leistenschollen". Teilweise grenzen diese Verwerfungen an kleine Sockelhebungen (z. B. das Kyffhäuser-Gebirge, der Bottendorfer Höhenzug und der Hornburger Sattel) oder an einzelne lokale Senken im Mesozoikum [Katzung und Ehmke, 1993]. Dabei zeigen Störungen in der Thüringer Mulde typischerweise niedrige Abschiebungs- und/oder Aufschiebungsversätze, die mit einer kompressiven Reaktivierung mesozoischer Abschiebungen während der späten Kreide zurückzuführen sind [vgl. Kley, 2013; Malz, 2014 und Referenzen darin].
Störungszonen des Thüringer Beckens
Faults of the Thuringian Syncline
Lauchstädt-Teutschenthal Fault Zone
The Lauchstädt-Teutschenthal fault zone forms a NW-SE trending fault system in southern Saxony-Anhalt.
Die Lauchstädt-Teutschenthaler Störungszone bildet eine NW-SE streichende Störungszone im Süden Sachsen-Anhalts.
Lauchstädt-Teutschenthaler Störungszone
Höhnstedt Fault Zone
The Höhnstedt fault zone forms a NW-SE-trending fault strand of the Lauchstädt-Teutschenthal fault zone.
Die Höhnstedt Störungszone bildet eine NW-SE-streichende Störungsspur der Lauchstädt-Teutschenthal Störungszone.
Höhnstedter-Störungszone
Höhnstedter Störung
Lauchstädt Fault Zone
The Lauchstädt-Teutschenthal fault zone forms a NW-SE trending fault in the south of Saxony-Anhalt with offsets of up to 500 m.
Die Lauchstädt-Teutschenthaler Störungszone bildet eine NW-SE streichende, etwa 500 m Sprunghöhe aufweisende Störung im Süden Sachsen-Anhalts.
Lauchstädt-Störungszone
Lauchstädt-Störung
Lützen-Zwenkau Fault Zone
The Lützen-Zwenkau fault zone forms a geophysically proven SW-NE trending fault in the southeast of Saxony-Anhalt in the border area to Saxony.
Die Lützen-Zwenkau Störungszone bildet eine geophysikalisch nachgewiesene SW-NE streichende Störung im Südosten Sachsen-Anhalts im Grenzbereich zu Sachsen.
Lützen-Zwenkauer StörungSzone
Finne Fault Zone
The Finne Fault Zone forms a NW-SE trending fault zone crossing the Thuringian Basin over a distance of 150 km. It forms the southwestern border of the Hermundurian Block and is interpreted as part of the seismically active Gera-Jáchymov zone.
Die Finne Störungszone bildet eine NW-SE-streichende, über 150 km verlaufende Störungszone im Norden des Thüringer Beckens. Sie bildet die südwestliche Grenze der Hermundurischen Scholle und wird als Teil der seismisch aktiven Gera-Jáchymov-Zone interpretiert.
Finne-Störungszone
Finne Störung
Kyffhäuser-Crimmitschau Fault Zone
The Kyffhäuser-Crimmitschau fault zone forms a significant NW-SE trending fault zone that separates the Hermundurian Block in the southwest from the Merseburg Block in the northeast. The offset is largest in the area of the Kyffhauser mountains. Interpreted as part of the Gera-Jáchymov zone, it still shows seismic activity today.
Die Kyffhäuser-Crimmitschau Störungszone bildet eine bedeutende NW-SE-streichende Störungszone, die die Hermundurische Scholle im Südwesten von der Merseburger Scholle im Nordosten trennt. Ihre größte Sprunghöhe zeigt die Störung im Bereich des Kyffhäusers. Als Teil der Gera-Jáchymov-Zone interpretiert zeigt sie immer noch seismische Aktivität in heutiger Zeit.
Kyffhäuser-Crimmitschau-Störung
Nienstedt-Eindorf Fault Zone
The Nienstedt-Eindorfer fault zone forms a NW-SE trending, SW-dipping fault in the central section of the Sangerhäuser Syncline. It reaches maximum offsets of up to 300 m.
Die Nienstedt-Eindorfer Störungszone bildet eine NW-SE streichende, nach Südwesten einfallende Störung im Zentralabschnitt der Sangerhäuser Mulde. Sie erreicht maximale Versätze von bis zu 300 m.
Nienstedt-Eindorfer Störung
Zwochau-Elstertal Fault Zone
The Zwochau-Elstertal Fault describes a system of fault zones that strikes almost north-south and separates the Halle Block from the Northwest Saxony Block.
Die Zwochau-Elstertal Störung beschreibt ein System von Störungszonen, die annähernd Nord-Süd streichen und die Halle Scholle von der Nordwestsächsischen Scholle trennen.
Zwochau-Elstertal-Störungszone
Elstertal Fault Zone
The Elstertal fault zone forms a fault branch of the Zwochau-Elstertal fault zone.
Die Elstertal Störungszone bildet einen Störungsast der Zwochaus-Elstertal Störungszone.
Elstertal-Störungszone
Zwochau Fault Zone
The Zwochau Fault Zone forms one fault strand of the Zwochau-Elstertal Fault.
Die Zwochau Störungszone bildet einen Störungsast der Zwochau-Elstertal Störungszone.
Zwochau-Störungszone
Hornburg Deep Fault System
The Hornburg Deep Fault System is a WSW-ENE trending fault zone in the north of the Thuringian Basin. It limits the Hornburger Sattel in the east. It shows offsets fluctuating over small distances reaching a maximum of 1500 m.
Die Hornburger Tiefenstörung ist eine WSW-ENE streichende Störungszone im Norden des Thüringer Beckens. Sie begrenzt den Hornburger Sattel im Osten. Sie zeigt kleinräumig schwankende und maximal 1500 m betragende Versätze.
Hornburger Tiefenstörung
Hettstedt Fault Zone
The Hettstedt fault zone describes a fault system in the area of the Halle-Hettstedt Anticline. This fault system separates the Subhercynian Basin from the Thuringian Basin and connects the basement uplifts of the Harz and the Halle-Wittenberg Block.
Die Hettstedt Störungszone beschreibt ein Störungssystem im Bereich der Halle-Hettstedter Gebirgsbrücke. Dieses Störungssystem trennt das Subherzyne Becken vom Thüringer Becken und verbindet die Grundgebirgsaufbrüche des Harzes und der Halle-Wittenberg-Scholle.
Hettstedt-Störungszone
Hettstedter Störung
Naumburg Fault Zone
The Naumburg fault zone is a NE-SW trending fault zone in the north-eastern Thuringia basin postulated on the basis of gravity gradient studies.
Die Naumburger Störungszone ist eine auf der Grundlage gravimetrischer Gradientenuntersuchungen postulierte NE-SW streichende Störungszone im nordöstlichen Thüringer Becken.
Naumburger Störungszone
Naumburg-Störung
Blankenheim-Geiseltal Fault Zone
The Blankenheim-Geiseltal fault zone describes the fault zone on the southern edge of the Hornburg anticline and its extension into the Geiseltal area in the southeast. It forms a fault zone that was already active in Permian times, which can be proven on the basis of differentiated sedimentation and magmatic activity.
Die Blankenheim-Geiseltal Störungszone bezeichnet die Störungszone am Südrand des Hornburger Sattels sowie ihre Verlängerung in den Bereich des Geiseltals im Südosten. Sie bildet eine bereits im Perm aktive Störungszone aus, was auf Basis differenzierter Sedimentation und magmatischer Aktivität belegt werden kann.
Blankenheim-Geiseltal-Störungszone
Geiseltal Fault Zone
The Geiseltal Fault forms the eastern section of the Blankenheim-Geiseltal Fault Zone.
Die Geiseltal Störung bezeichnet den östlichen Abschnitt der Blankenheim-Geiseltal Störungszone.
Geiseltal-Störungszone
Hornburg Anticline Southern Border Fault
The Hornburg Anticline Southern border fault forms the western section of the Blankenheim-Geiseltal fault zone. It delimits the Paleozoic units of the Hornburg Anticline in the north against the Mesozoic units of the Thuringian Basin in the south.
Die Hornburger Sattel Südrandstörung bildet den westlichen Abschnitt der Blankenheim-Geiseltal Störungszone. Sie begrenzt die paläozoischen Einheiten des Hornburger Sattels im Norden gegen die Mesozoischen Einheites des Thüringer Beckens im Süden.
Hornburger Sattel Südrand-Störung
Hornburg Fault
Hornburger Störung
Rosslau Fault Zone
The Rosslau fault zone is a NE-SW-trending fault that forms the southeastern border of the Flechtingen High against the Halle-Wittenberg Block in the pre-cenozoic subsurface. It forms the border between the Northern Phyllite Zone and the Central German Crystalline Zone.
Die Rosslau Störungszone ist eine NE-SW streichende Störung, die im präkänozoischen Untergrund die Südostgrenze der Flechtingen-Roßlauer Scholle gegen die Halle-Wittenberg Scholle bildet. Hierbei bildet sie die Grenze zwischen der Nördlichen Phyllitzone und der Mitteldeutschen Kristallinzone.
Rosslauer Störungszone
Rosslau-Störung
Halle Fault Zone
The Halle fault zone forms a W-E to NW-SE trending, slightly curved fault in the south of Saxony-Anhalt. It borders the Halle Porphyry Complex in the north against the Mesozoic strata of the northeastern Thuringian Basin in the south. With an offset of up to 1000 m, it forms one of the most significant fault zones in central Germany.
Die Halle Störungszone bildet eine W-E bis NW-SE streichende, leicht geschwungen verlaufende Störung im Süden Sachsen-Anhalts. Sie begrenzt den Halleschen Porphyrkomplex im Norden gegen die mesozoische Schichtenfolge des nordöstlichen Thüringer Beckens im Süden. Mit einem Versatz von bis zu 1000 m bildet sie eine der bedeutsamsten Störungzonen in Mitteldeutschland.
Hallesche Störungszone
Halle Fault
Hallesche Marktplatzverwerfung
All named tectonic boundary objects that are located (at least partly) in Portugal, are identified by an ID with the prefix „PT“ listed in the notation.
Falha em Portugal
Fault in Portugal displayed in the HIKE fault database and as they are represented on the Geological Map of Portugal at 1:1.000.000 scale.
Tectonic Boundary in Portugal
Seia-Lousã Fault
Lousã Fault
Falha de Lousã
Falha de Seia-Lousã
Extending between Lousã and Seia regions, this fault is a major structure limiting the Portuguese Central System in the north. It's interpreted as a late Variscan strike-slip, reactivated with an important reverse component, verging N, during the Mesozoic (Cretaceous) and the several Alpine compression episodes occurred in the Cenozoic. This fault conditions the occurrence of Caldas de S. Paulo water spring - Water temperature: 23º C.
This structure extend between Malpica (Spain) and Lamego (Portugal) regions and corresponds to an important shear zone with a complex tectonic history since pre‐Variscan to Variscan orogeny times. This structure conditions the occurrence of several water springs/sources - Water temperatures: < 20º C (Dossãos), 33º C (Caldelas), < 20º C (Giestal), 32º C (Caldas das Taipas), 50º C (Caldas de Vizela), 23º C (Caldas das Murtas/Pataratas), < 20º C (Varões).
Malpica-Lamego Fault
Falha de Malpica-Lamego
Segura Fault
Falha de Segura
This fault extends between Cegonhas Velhas and the Segura region, limiting, to the north, the Segura basin (Cenozoic), a subbasin located in the middle sector of the Lower Tagus Basin.
Ferrarias Antiform Fault
Falha do Antiforma de Ferrarias
This NW-SE structure is mapped along almost 3 km, next to Mina do Bugalho. It suffers a sinistral offset of about 2 km related with the Messejana Fault.
This fault is interpreted as a late Variscan sinistral strike-slip fault. This fault conditions the occurrence of several water springs - Water temperatures: 67º C (Termas de S. Pedro do Sul), < 20º C (Piar), < 20º C (Miguas/Ponte de Frende), 45º C (Caldas de Moledo) and 23º C (Seromenho).
Mesão Frio Fault
Falha de Mesão Frio
Ponsul Fault
Falha do Ponsul
In Portugal, the fault extends between Arneiro and Termas de Monfortinho areas. It's a late Variscan sinistral strike-slip fault, reactivated as a N verging reverse fault during the Cenozoic. It also coincides with the N limit of the Lower Tagus (Cenozoic) basin middle sector. It is one of the structures that accommodated the upflift of the Central System (Portuguese sector). This fault conditions the occurrence of Fonte das Virtdudes and Fonte Santa de Monfortinho water springs - Water temperatures: 21º C and 28º C, respectively.
This structure extends between Apúlia and Janarde areas, and is an important Variscan structure in the control of the Carboniferous basins, in the region.
Dúrico-Beirão Carboniferous Sulc Fault
Falha do Sulco Carbonífero Sulco-Beirão
This fault causes a sinistral offset on the Morais Complex, probably related with late Variscan deformation, and shows evidence of reverse behaviour in the Quaternary. This fault, in apparently conjunction with Morais Nappe Complex (PT-137), conditions the occurrence of Fonte da Abelheira and Escarledo water springs - Water temperature: < 20º C on both cases.
Morais Fault
Falha de Morais
Estremoz Antiform Fault
Carreamento do Antiforma de Estremoz
It extends along aproximately 40 km between Alandroal and Sousel areas. It's an interpreted structure, consisting in a deformed overthrust by the folding event responsible for the Estremoz Antiform formation.
This structure is a Variscan sinistral strike slip fault, reactivated along the Cenozoic with the same kinematic behaviour. This extensive structure conditions the occurrence of several water springs/sources - Water temperatures: 37º C (Unhais da Serra), 48º C (Caldas de Manteigas), < 20º C (Santo Amaro), < 20º C (Santo António), 34º C (Longroiva), 21º C (Currais do Leitão/Bem Saúde).
Manteigas-Vilariça-Bragança Fault
Falha de Manteigas-Vilariça-Bragança
Deixa-o-Resto Fault
Falha de Deixa-o-Resto
Probably extending from Melides to Sines (and further south to the offshore), this fault has strongly influenced the tectonic and stratigraphic evolution of the region. It's also one of the main structures controling the western slope of the Grândola range.
Grândola Fault
Falha de Grândola
This fault controls the northern face of the Grândola range, interpreted as a fault scarp. The real extension in unknown, however it is identifiable for about 45 km. It probably corresponds to an inherited variscan fault, reactivated with the alpine compression.
Carcavai Fault
Falha de Carcavai
Extending from Quarteira to São Brás de Alportel, it had an important role on the Algarve basin structuration during the Mesozoic. It was reactivated during the Cenozoic, related to the Alpine compression. This fault, in conjunction with the São Marcos-Quarteira Fault (PT-004), conditions the occurrence of Fonte Santa (Quarteira) water spring - Water temperature: 21º C.
Lower Tagus Valley Fault System
Sistema de falhas do Vale Inferior do Tejo
Lower Tagus Valley FS is an important structure in the genesis and evolution of the intermediate sector of the Cenozoic Lower Tagus basin. Its extension is uncertain because a major part of its course follows the present Tagus river channel, hidden bellow recent alluvium.
Santa Iria Fault
Falha de Santa Iria
Mapped between São João da Talha e Vialonga areas, this fault is part of an important fault system in the tectono-stratigraphic evolution of the Cenozoic Lower Tagus basin. Apparently, this fault, in conjuction with Vila Franca de Xira Fault (PT-006-2), conditions the occurrence of Mouchão da Póvoa water spring - Water temperature: < 20º C.
Vila Franca de Xira Fault
Falha de Vila Franca de Xira
This fault is mapped between Alverca do Ribatejo and Carregado areas. Part of it extends below the Tagus river alluvium. It was an important fault accomodating the Mesozoic extension, as a normal fault, and was tectonically inverted during the Cenozoic as a reverse fault. Apparently, this fault conditions the occurrence of Mouchão da Póvoa water spring: water temperature < 20º C.
Azambuja Fault
Falha da Azambuja
It enxtends from Azambuja to Almoster area (uncertain extension) and had an important role in the structuration of the Lower Tagus basin during the Cenozoic.
Ribeira de Telhares Fault System
Sistema de Falhas da Ribeira de Telhares
A fault system that extends between Nave Redonda and Corte de Briques. There are a group of tectonic depressions related to its activity along the Neogene and early Pleistocene, with clear morphological expression.
Mendiga-Reguengo do Fetal Fault System
Mendiga – Reguengo do Fetal fault system is inherited from late Variscan deformation. After Lower Cretaceous, Reguengo do Fetal fault behaved as a normal fault and Mendiga fault has a strike-slip. Apparently, this system fault conditions the occurrence of Lena and Liz karstic springs on Maciço Calcário Estremenho aquifer system - Water tempertures: < 20º C on both cases.
Mendiga Fault
Falha da Mendiga
Reguengo do Fetal Fault
Falha do Reguengo do Fetal
Vale de Fecho Fault
Falha de Vale de Fecho
This fault extends approximately 14 km to the south, from São Teotónio. Its total extension is unknown. The deformation is directly expressed by one outcrop showing a fault zone affecting Plio-Quaternary continental sediments, and by the existence of a tectonic depression filled with Neogene and early Quaternary sediments.
Alvados-Minde Fault System
Sistema de falhas de Alvados-Minde
Alvados – Minde fault system separates Santo António plateau from Aire mountain range and São Mamede plateau, creating a deep depression in the Alvados and Minde area. The system functioned as normal fault during the Mesozoic distensive period leading to the roll-over structuring of São Mamede Plateau, being subsequently reactivated as a dextrogira lateral ramp of the Arrife thrust during the miocene inversion period. This fault system conditions the depressions of Alvados and Minde which, due to the various temporary karstic springs and swallow holes that occur there, constitute both recharge zones and discharge zones of the Maciço Calcário Estremenho aquifer system, the bigger and the most important karstic aquifer of Portugal - Water temperatures: < 20º C on all cases.
Alvados Fault
Falha de Alvados
Minde Fault
Falha de Minde
Torrão Fault
Falha de Torrão
Extending between Cuba and Vale de Arca areas, it was an important structure in the genesis and evolution of the Cenozoic Alvalade basin.
Vidigueira-Moura Fault
Falha de Vidigueira-Moura
The fault extends about 65 km between Vidigueira and Moura. It acted as a sinistral strike-slip during the late Variscan fragile regime and was reactivated several times in the Cenozoic in relation with the Alpine orogeny, controling the tectonostratigraphic evolution of the Cenozoic Moura basin. Apparently, this fault not conditions the water sources of Termas de Moura located on the south of it - Water temperature: 22º C.
This correspond to a complex of nappes limited by overthrusts, consisting in a series of allocthonous and parautocthonous units emplaced over the Iberian Terrane during the Variscan orogeny.
Morais Nappe Complex
Complexo de Nappes de Morais
Amareleja Fault
Falha de Amareleja
This fault extends about 9 km between Amareleja and Póvoa. It seems responsible for the existence of a small tectonic scarp and controlled the neogenic sedimentation on the southern footwall block. ic evolution of the Cenozoic Lower Tagus basin. This fault conditions the occurrence of Fonte Santana water spring - Water temperature: < 20º C.
This fault is a Variscan thrust.
Vila Verde Fault
Falha de Vilaverde
Cercal Anticline Fault
Falha do Anticlinal do Cercal
This SW verging reverse fault is located along the western flank of the Cercal Anticline.
This is a main structure separating the Central Iberian Zone and the Galicia - Trás-os-Montes Zone. This structure conditions the occurrence of Moimenta da Raia, Terronha and Lagoaça water springs - Water temperature: < 20º C, on all cases. It conditions too the Carvalhelhos spring - Water temperature: 22 ºC.
Trás-os-Montes Main Thrust
Cavalgamento principal de Trás-os-Montes
Lousal-Caveira Anticline Fault
Falha do Anriclinal de Lousal-Caveira
This SW verging reverse fault corresponds to a rupture along the SW flank of the Lousal-Caveira Anticline.
This correspond to a complex of nappes limited by overthrusts, consisting in a series of allocthonous and parautocthonous units emplaced over the Iberian Terrane during the Variscan orogeny. This structure conditions the occurrence of Santa Cruz water spring - Water temperature: < 20º C.
Bragança Nappe Complex
Complexo de Nappes de Bragança
This fault is interpreted as a Variscan strike-slip. This fault conditions the occurrence of Alfaião water spring - Water temperature: < 15º C.
Vale de Asnes-Faílde Fault
Falha de Vale de Asnes-Faílde
Castelo de Vide Fault
Falha de Castelo de Vide
This fault is mapped between Santo Amaro and Meada areas, along 60 km, and is probably a late hercynian or alpine left-lateral strike slip fault, cutting through all the hercynian structure. At Castelo de Vide, a sinistral offset of about 300 m can be seen, affecting Ordovician quartzites. This fault conditions the occurrence of some water springs in Termas de Castelo de Vide (Fonte da Vila, Fonte Mealhada) and Cabeço de Vide (Termas da Sulfúrea) - Water temperatures: < 20º C on all cases.
This fault is interpreted as a oblique dextral late Variscan strike-slip. It conditions the occurrence of Alfaião water spring - Water temperature: < 15º C.
Aveleda-Gimonde Fault
Falha de Aveleda-Gimonde
Terena Thrust
Terena Overthrust
Carreamento de Terena
Cavalgamento de Terena
This fault is a Variscan structure located in the Barrancos-Elvas sector of the Ossa Morena Zone.
Juromenha Thrust
Carreamento da Juromenha
Cavalgamento da Juromenha
This fault extends between the Alter do Chão and Juromenha regions. It is considered an important structure in the Ossa Morena Zone, separating the Cambrian units of Alter do Chão-Elvas from Silurian rocks of Estremoz-Barrancos sectors.
This fault is interpreted as a normal intra-orogenic fault with a sinistral component, during the Variscan orogeny.
Pena Suar Fault
Falha de Pena Suar
Messejana Fault
Odemira-Ávila Fault
Falha de Odemira-Ávila
Falha da Messejana
Extending about 250 km in Portugal (500 km in total), between São Teotónio and Campo Maior, it is the largest mapped fault in Portugal. Its fault trace frequently coincides with an igneous dyke intruded during the Lower Jurassic. It had an important role on the tectonic genesis and evolution of the Cenozoic Alvalade basin. This fault conditions the occurrence of Fonte da Graça (Ouguela) and S. João do Deserto (Aljustrel) water springs - Water temperatures: < 20º C on both cases.
Alter do Chão Fault
Falha de Alter do Chão
This fault corresponds to the northern border of the Alter do Chão-Elvas, in the Ossa Morena Zone domain. To the north there's the Tomar-Badajoz-Córdoba Shear Zone. It is recognized along aproximately 25 km, between Monforte and Alter do Chão regions.
This fault extends between the Vinhais and Bragança areas and is a Variscan sinistral strike-slip fault. This fault, in apparently conjunction with Bragança Nappe Complex (PT-136), conditions the occurrence of Castro de Avelãs water spring - Water temperature: < 20º C.
Vinhais Fault
Falha de Vinhais
São Teotónio-Aljezur-Sinceira Fault System
Sistema de falhas de São Teotónio-Aljezur-Sinceira
It extends about 45 km between Sagres and São Teotónio, where it connects to the Messejana fault. Along the fault trace there are several tectonic depressions related to its strike-slip kinematics during the Cenozoic. This fault conditions the occurrence of Sinceira (Vila do Bispo) water spring - Water temperature: < 20º C.
Maranhão Fault
Falha do Maranhão
This fault is interpreted as a late Hercynian reverse fault that was reactivaded as a right-lateral strike slip during the Alpine compression. Altough related deformation was recognized from Montargil lake to about 30 km to SE, its total lenght is still uncertain.
This fault is interpreted as a Variscan strike-slip. It conditions the occurrence of Fonte Santa do Seixo, Lagarteira and, apparently, Caldas da Cavaca water springs/sources - Water temperatures: 21º C, < 20º C and 29º C, respectively.
Vila Flôr-Aguiar da Beira Fault
Falha de Vila Flôr-Aguiar da Beira
São Marcos-Quarteira Fault
Falha de São Marcos Quarteira
Extending from Quarteira to São Marcos da Serra it had an important role on the Algarve basin structuration during the Mesozoic. It was reactivated during the Cenozoic in relation to the Alpine compression. This fault, in conjunction with the Carcavai Fault (PT-005), conditions the occurrence of Fonte Santa (Quarteira) water spring - Water temperature: 21º C.
Santo Aleixo da Restauração Thrust
Santo Aleixo da Restauração Overthrust
Carreamento de Santo Aleixo da Restauração
Cavalgamento de Santo Aleixo da Restauração
It's a major structure in the Ossa Morena Zone, separating the Montemor-Ficalho and Estremoz-Barrancos sectors.
This fault is interpreted as a late Variscan sinistral strike-slip. It conditions the occurrence of Cótimos and Vilares water springs - Water temperatures: < 20º C on both cases.
Santa Comba-Covilhã Fault
Falha de Santa Comba-Covilhã
Arrife Fault
Falha do Arrife
From Casais Monizes to Serra de Baixo, it had an important role in the fracturation of Pangea and the opening of the Atlantic as a normal fault; has been reactived as strike-slip with reverse component during the Alpine orogeny, promoting the Lusitanian basin Inversion. This fault conditions the occurrence of Alviela and Almonda water springs, the two most flowing karstic exsurgencies of Portugal - Water temperatures: < 20º C on both cases.
Quiaios Fault
Falha de Quiaios
This fault extends between Ereira and Murtinheira. It is a local structure that accommodated the shortening promoted by the Alpine compression.
Celorico de Basto Nappe Complex
Complexo de Nappes de Celorico de Basto
Falha de Vila Verde
Vila Verde fault
NNW-SSW fault, extending from the coast, near Caldas da Rainha, to SSW until the Tagus river, close to Vila franca de Xira. This fault conditions the occurrence of Convento da Visitação water spring - Water temperature: < 20º C.
This fault is interpreted as a late Variscan sinistral strike-slip. Apparently, this fault conditions the occurrence of Caldas de Carlão, Caldas de S. Lourenço and Ponte do Fumo water springs - Water temperatures: 29ºC (Carlão), 30º C (S. Lourenço) and < 20º C (Ponte de Fumo).
Castanheiro do Norte-Nagozelo Fault
Falha de Castanheiro do Norte-Nagozelo
N-S Fault that borders the Ariques Mountain range. It is a major listric fault parallel to Porto-Tomar Fault which is the boundary of Lusitanian Mesozoic basin
Alvaiázere Fault
Falha de Alvaiázere
This fault corresponds to the Ossa Morena Zone/Central Iberian Zone in the Tomar-Sardoal-Ferreira do Zêzere sector.
Ortiga-Torrão Fault
Falha de Ortiga-Torrão
Condeixa Fault
Falha de Condeixa
This fault extends through Condeixa city until Coimbra city. It is a normal fault that originated in the opening of the Lusitanian Basin.
This structure extends between the Casal da Igreja and Sardoal areas and marks the boundary between the Fontes metagraywacks and phyllites, and the Mouriscas Gnaissic Complex.
Casal da Igreja-Sardoal Fault
Falha de Casal da Igreja-Sardoal
This fault crosses Alegrete village. It is a transcurrent fault of the southern border of the Centro Iberica tectonostratigraphic zone.
Alegrete Fault
Cavalgamento de Alegrete
N-S oriented Fault that borders the Alvaiázere Mountain range. It is a major listric fault parallel to Porto-Tomar Fault, which is the boundary of Lusitanian Mesozoic basin. This fault conditions the occurrence of Agroal water spring - Water temperature: < 20º C.
Ariques Fault
Falha de Ariques
This transcurrent fault extends between Crato and Campo Maior, and is one of the major faults that defines the Coimbra-Cordoba Shear Zone, wich makes the frontier between Ossa Morena and Centro Ibérica tectono stratigraphic zone of tha Iberian Massif.
Mosteiros Fault
Falha de Mosteiros
This fault extends between Portalegre city and Esperança village. It is a transcurrent fault of the southern border of Centro Iberica tectonostratigraphic zone.
Portalegre-Esperança Fault
Cavalgamento de Portalegre-Esperança
Campo Maior fault is one of the southern faults of the Coimbra-Cordoba shear zone wich makes the frontier between Ossa Morena and Centro Ibérica tectono stratigraphic zones of tha Iberian Massif.
Campo Maior Fault
Falha de Campo Maior
Ouguela fault is one of the southern faults of Coimbra-Cordoba shear zone wich makes the boundary between Ossa Morena and Centro Ibérica tectono stratigraphic zones of the Iberian Massif. This fault, in conjunction with the Messejana Fault (PT-002), conditions the occurrence of Fonte da Graça (Ouguela) water spring - Water temperature: < 20º C .
Ouguela Fault
Falha de Ouguela
Pedrogão fault
Falha de Pedrogão
The fault crosses the locality of Pedrogão. It acted as a sinistral strike-slip during the late Variscan fragile regime and was reactivated several times in the Cenozoic in relation with the Alpine orogeny.
Martinhal Fault
Falha de Martinhal
This fault is observed at Martinhal beach, near Sagres, consisting of a reverse fault affecting Upper Jurassic and Pliocene-Pleistocene sands. Measured striae also point to the existence of dextral movement.
This fault is interpreted as a Variscan dextral strike-slip.
Outeiro-Avinhó Fault
Falha de Outeiro-Avinhó
Monte Figo Fault
Falha de Monte Figo
The fault extends in about 10 km between Estói and Moncarapacho. It is interpreted as a northwards directed thrust and the existence of sheared and folded Upper Jurassic beds overlain by undeformed Lower Cretaceous indicates a compressive episode on the Jurassic/Cretaceous boundary, intercalated in a distensive regime. Apparently, in conjuction with Silves Benaciate Fault (PT-112), it conditions the occurrence of Olheiros water spring - Water temperature: <20º C.
This fault is interpreted as a Variscan fragile structure.
Alfândega da Fé-Almendra Fault
Falha de Alfândega da Fé-Almendra
This structure is a main fracture zone in Iberia, establishing the boundary between the Ossa Morena Zone and Central Portuguese Zone, in its northern sector, and the boundary between the Ossa Morena Zone and the South Portuguese Zone, in its southern sector. This structure conditions the occurrence of some water spring/sources - Water temperatures: 23º C (Caldinhas de Vilar), 23º C (Caldas de S. Jorge), < 15º C (Vale da Mó), 27º C (Termas de Luso) and < 20º C (Foz do Sertã).
Porto-Tomar-Ferreira do Alentejo Shear Zone
Zona de Cisalhamento Porto-Tomar-Ferreira do Alentejo
This fault presented extensional kinematic during the Mesozoic and was reactivated in the Cenozoic as a left lateral strike-slip fault.
Pinhal Novo-Alcochete Fault
Falha de Pinhal Novo-Alcochete
This fault is interpreted as a Variscan sinistral strike-slip.
Praia Norte fault
Falha de Praia Norte
Vilarouco-Vale de Janeiro Fault
Falha de Vilarouco-Vale de Janeiro
Alcoutim Fault
Falha de Alcoutim
NE-SW cenozoic fault that extends throught Pomarão anticline
Occurring next to Antas, this fault is part of a set of structures that delimit fragments of oceanic lithosphere (ophiolite sequences).
Antas Fault
Falha de Antas
Ferreira-Pias Fault
Falha de Ferreira-Pias
The fault extends between Ferreira do Alentejo and Pias. It acted as a sinistral strike-slip fault during the late Variscan fragile regime and was reactivated several times in the Cenozoic in relation with the Alpine orogeny.
Occurring near Santana, this fault is part of a set of structures that delimit fragments of oceanic lithosphere (ophiolite sequences).
Santana Fault
Falha de Santana
Neves Corvo Thrust
Cavalgamento de Neves Corvo
This thrust limit the southern limb of Rosario anticline where the Neves Corvo mine is located.
Ribeira de Vascão Fault
Falha da Ribeira do Vascão
NE-SW cenozoic fault of the Pomarão anticline that extends along the Vascão stream. This fault conditions the occurrence of Águas Santas de Besteiros (Vascão) water spring - Water temperature: 21º C.
Occurring next to Vila Ruiva, this fault is part of a set of structures that delimit fragments of oceanic lithosphere (ophiolite sequences).
Vila Ruiva Fault
Falha de Vila Ruiva
Mértola Thrust
Cavalgamento de Mértola
Limits the Mértola nappe at the South Portuguese tectono stratigraphic zone. This thrust conditions the occurrence of Mértola and Água Santa da Morena water springs - Water temperatures: < 20º C on both cases.
Castro Verde Thrust
Cavalgamento de Castro Verde
The Castro Verde thrust limits a major anticline near Castro Verde village, where Neves-Corvo mine is located.
Pulo do Lobo Thrust
Cavalgamento de Pulo do Lobo
This thrust makes the south limit of Pulo do Lobo accretionary terrane at the South Portuguese tectono stratigraphic zone
Galé Thrust
Cavalgamento da Galé
Limits the Galé-Cela nappe at the South Portuguese tectono stratigraphic zone
Viso Fault
Falha do Viso
Major thrust of the Viso assymmetric anticline, northwest of Setúbal.
Ferreira-Ficalho Thrust
Cavalgamento de Ferreira Ficalho
Major thrust that mark the boundary between Ossa Morena and South Portuguese tectono-stratigraphic zones. This boundary corresponds to a Variscan suture between the Iberian and Avalonia terranes and was first interpreted as corresponding to the Beja-Acebuches Ophiolitic Complex. It extends from the spanish border (Ficalho) to west, near Ferreira do Alentejo.
São Brás de Alportel fault
Falha de São Brás de Alportel
The fault extends between Alportel and Aceifãos. It has morphological expression represented by a scarp, facing S, and accommodated part of the Caldeirão range uplift, during the Quaternary.
Albufeira Fault
Falha de Albufeira
This fault extends between Ponta da Baleeira and Mourição. It accommodated the Mesozoic extension as a normal fault and was tectonically inverted during the Cenozoic, as a left lateral strike slip. It's an important structure controlling local diparism (the Albufeira diapir).
Baleeira Fault
Falha da Baleeira
The fault extends between Albufeira and Pêra, approximately. It accommodated the Mesozoic extension as a normal fault and was tectonically inverted during the Cenozoic, as a reverse dextral fault.
Faro Fault
Falha de Faro
The extension of this fault is unknown. It was inferred from geophysical data and sedimentary facies analysis. It's an important structure in the control of local diapirism.
Loulé fault
Falha de Loulé
Extending between Loulé and Boliqueime, the Loulé fault behaved as a normal fault during the Mesozoic extensive and as a sinistral normal fault in the Pleistocene.
Lagos Fault
Porto de Mós Fault
Falha de Porto de Mós
Falha de Lagos
The fault extends from Canelas to Porto de Mós beach, where a reverse fault affecting Cretaceous and Miocene sediments can be observed. It behaved as a normal fault during the Mesozoic.
Portimão Fault
Falha de Portimão
From Guenos to Praia da Rocha (Portimão) in Portugal mainland, this fault extends further south to the offshore. It is interpreted as a late Variscan structure reactivated during the Mesozoic and Cenozoic. Apparently, thid fault, in conjuction with Silves Benaciate Fault (PT-112), conditions the occurrence of Seixosas/Ferragudo water spring - Water temperature: < 20º C.
Barão de São João Fault
Falha de Barão de São João
It extends between Candeira and Ponte da Torre and one of its main characteristic consists in a well preserved fault scarp.
Espiche-Odiáxere Fault
Falha de Espiche-Odiáxere
The fault extends from Burgau to Monte Judeu. It accommodated the Mesozoic extension as a normal fault and was tectonically inverted during the Cenozoic, as a reverse fault. It conditions the Salema, Valverde and Meia Praia water springs - Water temperatures: < 20º C on all cases.
This structure is located in the Olalhas area and corresponds to a tectonic klippe.
Olalhas Fault
Olalhas Klippe
Klippe de Olalhas
Falha de Olalhas
This fault extends between the Rosmaninhal and Casal Novo areas.It is related with Variscan deformation in the meridional sector of the Central Iberian Zone.
Rosmaninhal-Casal Novo Fault
Falha de Rosmaninhal-Casal Novo
This fault extends between the São José das Matas and Gargantada areas. It is related with Variscan deformation in the meridional sector of the Central Iberian Zone.
São José das Matas-Gargantada Fault
Falha de São José das Matas-Gargantada
This structure is part of a corridor of ductile deformation known as the Montemor-o-Novo Shear Zone.
Casa Branca Shear Zone
Zona de Cisalhamento de Casa Branca
Eira de Agosto Fault
Falha de Eira de Agosto
The fault extends between Alportel and Carrasqueiro. It has a morphological expression represented by a scarp, facing SW, and accommodated part of the Caldeirão range uplift, during the Quaternary.
This fault extends between the Queixopêrra and Louriceira areas.It is related with Variscan deformation in the meridional sector of the Central Iberian Zone.
Queixopêrra-Louriceira Fault
Falha de Queixopêrra-Louriceira
Santo Estevão Fault
Falha de Santo Estevão
The extension of this fault is unknown but it probably extends between the Olhão and Castro Marim areas. This fault conditions the occurrence of Santo António/Atalaia and Fonte Salgada water springs - Water temperature: 25º C and < 20º C, respectively. Apparently, in conjuction with Monte Figo Fault (PT-023), this fault conditions too the Olheiros water spring - Water temperature: < 20º C.
Occurring next to Oriola, this fault is part of a set of structures that delimit fragments of oceanic lithosphere (ophiolite sequences).
Oriola Fault
Falha de Oriola
This structure is the northern limit of a corridor of ductile deformation known as the Montemor-o-Novo Shear Zone.
Boa Fé Shear Zone
Zona de Cisalhamento de Boa Fé
São Luís Fault
Cavalgamento de São Luís
Major thrust of the São Luís assymmetric anticline, northwest of Setúbal.
This structure is a SW verging thrust that occurs along the NE flank of the Vila Velha de Ródão syncline. It is related with the Variscan orogeny deformation.
Chão das Servas-Carregais Fault
Falha de Chão das Servas-Carregais
Palmela Fault
Escama de Palmela
Gravitational Collapse structure near Palmela village.
This fault, with unknown extension, is interpreted as Variscan lateral ramp reactivated as a dextral strike-slip during the late Variscan tectonic episodes.
Sobral Fernando Fault
Falha de Sobral Fernando
Vale do Brejo-Frade-Zambujal Fault
Falha de Vale do Brejo-Frade-Zambujal
NW-SE fault diverging radially from the Sesimbra diapiric structure.
Galapos Fault
Falha de Galapos
Galapos Fault is a major thrust extending from Galapos beach to Risco, to the west.
Cova da Mijona Fault
Falha da Cova da Mijona
This fault is one of the Cova da Mijona dome border, west of Sesimbra village.
Sesimbra-Santana Fault
Falha de Sesimbra-Santana
Major fault bordering the Sesimbra diapiric structure.
Ajuda Fault
Falha da Ajuda
Strike slip fault extending throught the western sector of Lisbon.
Forte da Baralha Fault
Falha do Forte da Baralha
This fault is the west border of Forte da Baralha horst, near Espichel cape.
São Julião-Barcarena Fault
Falha de São Julião-Barcarena
Normal fault crossing the city of Oeiras.
This fault extends between the Silves and Benaciate areas. Apparently, in conjuction with Porimão Fault (PT-012), it conditions the occurrence of Seixosas/Ferragudo water spring - Water temperature: < 20º C
Silves-Benaciate Fault
Falha de Silves-Benaciate
This fault is mapped between the Trigaches and Monte da Barrada areas, north of Ferreira do Alentejo.
Peroguarda Fault
Falha de Peroguarda
This fault is mapped between the Algibre and Querença areas, in Algarve. It behaved as a normal fault during the Mesozoic and suffered tectonic inversion, as a reverse fault, during the Cenozoic Alpine compression. This fault system conditions the occurrence of Benémola water spring - Water temperature: < 20º C.
Algibre Fault System
Algibre Fault
Falha de Algibre
Sistema de falhas de Algibre
Carvalhal-Amendoeira Fault
Falha de Carvalhal-Amendoeira
This fault extends between Assumada and Freixo Seco, Algarve. It's a north verging reverse fault, affecting the Triassic Silves Formation and the Carboniferous Mira Formation.
Assumadas-Freixo Seco Fault
Falha de Assumadas-Freixo Seco
This fault extends between São Brás de Alportel and Julião, in Algarve. It is probably related with the basin inversion episodes related with the Alpine orogeny.
São Brás de Alportel-Julião Fault
Falha de São Brás de Alportel-Julião
El Carmen Fault
Falha de El Carmen
El Carmen Fault is mainly a normal fault, being reactivated as a thrust in the Miocene Alpine orogeny. It extends northwards, from Galapos beach.
This fault is the northern limit of the Cenozoic Sarzedas basin (subbasin of the Lower Tagus basin) and was active during the Neogene compressive episodes related to the Alpine orogeny. It is one of the structures that accommodated the upflift of the Central System (Portuguese sector). This fault conditions the occurrence of Foz do Cobrão water spring - Water temperature: 20º C.
Galdins-Rapoula-Chão da Vã Fault
Falha de Galdins-Rapoula-Chão da Vã
This fault is one of the main structures that accommodated the upflift of the Portuguese Central System in its southern sector.
Sobreira Formosa-Grade-Sobral do Campo Fault
Falha de Sobreira Formosa-Grade-Sobral do Campo
Sintra Fault System
Sistema de Falhas de Sintra
Sintra/Galamares Thrust
Cavalgamento de Sintra/Galamares
Sintra/Galamares thrust is north vergent and was formed during the cenozoic tectonic inversion.
São João das Lampas Thrust
Cavalgamento de São João das Lampas
São João das Lampas thrust verges to the north and was formed during the cenozoic tectonic inversion.
Buçaco-Penedo de Góis Fault
Falha de Buçaco-Penedo de Góis
This fault extends along the Buçaco-Penedo de Góis syncline, controlling its SW flank.
Dona Maria Fault
Falha de Dona Maria
The Dona Maria fault extends from Almargem do Bispo to south of Dona Maria village.
Sobral Fault
Falha do Sobral
Sobral fault is a major normal fault that intersects the Upper Jurassic Arruda sub-basin near Sobral de Monte Agraço village. This fault is in continuity with Santa Iria fault (PT006-3).
Almargem do Bispo Fault System
This N-S fault system is an extensional structure formed during the cenozoic inversion tectonic event.
Almargem do Bispo Fault
Falha de Almargem do Bispo
This structure is, possibly, a conjugate of the Cortegaça fault, and extends from Almargem do Bispo to near Negrais.
Pero Pinheiro Fault
Falha de Pero Pinheiro
This structure extends between the areas of Almargem do Bispo and Sobral da Abelheira.
Cortegaça Fault
Falha de Cortegaça
This structure is paralel to Pero Pinheiro fault and extends between A-dos-Francos and the Enxara do Bispo area.
This structure is a NE verging thrust that occurs along the SW flank of the Vila Velha de Ródão syncline. It is related with the Variscan orogeny deformation. This fault, in apparently conjunction with Galdins-Rapoula-Chão da Vã Fault (PT-106), conditions the occurrence of Foz do Cobrão water spring - Water temperature: 20º C.
Vinagra-Foz do Cobrão Fault
Falha de Vinagra-Foz do Cobrão
This fault extends between the Penacova (Portugal) and Verín (Spain) regions and is interpreted as a late Variscan sinistral strike-slip fault, reactivated in the Cenozoic during the Alpine compression with the same kinematics. This extensive structure conditions the occurrence of several water springs/sources (Caldas de Penacova, Termas do Carvalhal; Pedras Salgadas, Vila Verde/Areal, Fonte Salus, Termas de Vidago, Caldas de Chaves and Vilarelho da Raia) - Water temperatures: <20º C (Penacova), 41º C (Carvalhal), <20º C (Pedras Salgadas), <15º C (V. Verde/Areal), <20º C (Fonte Salus); <15º C (Termas de Vidago), <77º C (Chaves), <20º C (Vilharelho).
Penacova-Régua-Verín Fault
Falha de Penacova-Régua-Verín
This fault extends along the quartzite crest of Monforte da Beira, affecting Cambrian and Ordovician rocks.
Monforte da Beira Fault
Falha de Monforte da Beira
This structure occurs along the NE flank of the Serra do Moradal-Fajão Variscan syncline.
Pé da Serra-Cartamil Fault
Falha de Pé da Serra-Cartamil
This structure extends along the SW flank of the Serra do Moradal-Fajão Variscan syncline.
Vilar Barroco-Fajão Fault
Falha de Vilar Barroco-Fajão
This fault has unkown extension and is interpreted as a Variscan sinistral strike-slip fault.
Ademoço Fault
Falha de Ademoço
This fault is interpreted as a late Variscan strike-slip fault causing a dextral offset on the Serra do Moradal-Fajão syncline.
Cebola Fault
Falha de Cebola
S. Pedro Dias-Segade Fault
Falha de S. Pedro Dias-Segade
Extending between S. Pedro Dias and Segade areas, this structure is related with an important compression episode in the Alpine orogeny context.
Cascais Fault
Falha de Cascais
This dextral srike slip fault extends from Cascais to NW, near Guincho beach. Apparently, this fault conditions the occurrence of Termas do Estoril water springs/sources - Water temperature: 35º C.
This fault extends between Meãs and Senhora da Peneda, and is related with the Portela de Unhais quartzite ridge.
Portela de Unhais Fault
Falha de Portela de Unhais
Gerês-Lobios Fault
This fault is an important fracture, well represented in the morphology by a long straight valley. It conditions the occurrence of Caldas do Gerês water spring - Water temperature: 47º C .
Tojeira Fault
Falha de Tojeira
Thrust fault located west of the Montejunto anticline. This fault, in conjunction with the Vila Verd Fault (PT-049), conditions the occurrence of Convento da Visitação water spring - Water temperature: < 20º C.
Runa Fault System
Runa Fault
Falha de Runa
N-S trending fault that establishes the west boundary of the Cretaceous Runa sub-basin. This sub-basin separates the Upper Jurassic sub-basins of Arruda and Turcifal.
Sizandro Fault
Falha do Sizandro
Areeiro Fault
Falha de Areeiro
Fault affecting the northern limb of Montejunto anticline.
Rocha Forte Fault
Falha de Rocha Forte
This thrust fault is located at the northen sector of the Montejunto Structure and has a vergence to the north.
Torres Vedras Fault
Falha de Torres Vedras
E-W fault near Torres Vedras city, extending to the east until the Montejunto Mountain range. Main movement as normal fault in relation with the Mesozoic Atlantic opening, later reactivated as a reverse fault during the Alpine orogeny. This fault conditions the occurrence of Cucos water spring group - Water temperature: 40º C.
Cercal-Candeeiros Fault
Falha de Cercal-Candeeiros
This fault extends between the Montejunto and Candeeiros mountain ranges. It behaved as a normal fault during the Mesozoic Atlantic opening, later reactivated as a reverse fault during the Alpine orogeny.
Lourinhã Fault
Falha da Lourinhã
NNE-SSW trending fault, extending from Serra del Rei to near de Vimeiro diapir, to the south. The Lourinhã fault is rooted in the paleozoic basement as showed by seismic profiles. This fault conditions the occurrence of Vimeiro water spring group - Water temperature: 26º C.
Sapataria Fault
Falha da Sapataria
N-S normal fault extending between Sapataria and Lousa villages.
Caldas da Rainha diapiric structure
Estrutura diapirica de Caldas da Rainha
This structure extends from the area of Valado dos Frades until the south of Óbidos. Its eastern sector limits the western border of Estremenho Limestone Massif, in the so-called Bombarral Basin - Alcobaça. The Caldas da Rainha Diapiric structure was active during the Cenozoic. This diapiric structure conditions the occurrence of Caldas da Rainha, Óbidos (Gaeiras), Salir do Porto and Águas Santas water springs - Water temperatures: 36º C (Caldas da Rainha), 29º C (Óbidos), 20º C (Salir do Porto) and < 20º C (Águas Santas).
Nazaré Fault
Falha da Nazaré
Nazaré Fault is a first order tectonic strtucture wich separates two differente domains of Lusitanian basin. This fault extends from the Nazaré region, on the coast, to Pombal. This fault conditions the occurrence of Piedade, Fonte Quente and Porto Moniz water springs - Water temperatures: 27º C (Piedade), 24º C (Fonte Quente) and < 20º C (Porto Moniz).
Candeeiros Fault
Falha de Candeeiros
It behaved as a normal fault at least during the Middle Jurassic. Its southernmost section was reactivated during the Miocene. It extends from the east region of Évora de Alcobaça to near Porto de Mós, to the north.
Cidral Fault
Falha do Cidral
This structure limits the Pliocene Rio Maior Basin to the East. It is related with diapiric tectonics and behaved as a normal fault during the Pliocene.
Rio Maior-Porto de Mós Fault
Falha de Rio Maior-Porto de Mós
The Rio Maior-Porto de Mós fault is a major fault rooted in the paleozoic basement. Its reactivation and the existent diapiric structure are related. This fault conditions the occurrence of Salgadas (Batalha) and Fonte da Pipa (Rio Maior) water springs/sources - Water temperatures: 23º C (Salgadas) and < 20º C (Fonte da Pipa).
Ferrel Fault
Falha de Ferrel
This fault extends along the coast line located north of Peniche (near Ferrel).
Abrã Fault
Falha de Abrã
N-S Fault that intersects the igneous breccia of Abrã
Turquel Fault
Falha de Turquel
NW-SE fault that crosses the Caldas da Rainha diapiric structure extending from Famalicao (NW) to Turquel and Benedita (SE).
Prelomi v Sloveniji
Tectonic Boundary in Slovenia
All named tectonic boundary objects that are located (at least partly) in Slovenia, are identified by an ID with the prefix „SI“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Slovenia displayed in the HIKE European fault database. Information on faults in Slovenia are based on the map and database of active faults in Slovenia (MAF.SI) which includes all known active, probably active and potentially active faults with surface fault traces >5 km in length.
Pölsko-Labotski prelomni sistem
Pöls-Lavanttal Fault System
This ca. 150 km long, approximately NW-SE, partly NNW-SSE trending Fault System extends from the Pöls Valley (south of Trieben) to Judenburg and Obdach, following the Lavant Valley to Lavamünd (Labot) and Drauburg (Dravograd) and the Mislinja Valley (SLO) to Slovenske Konjice (south of the Pohorje Mountains). There it is cut by the Sava-Celje-Faultsystem. It includes the Pöls (Decker et al. 1994), Lavanttal Subfault Systems (Linzer et al., 2002; Kurz et al., 2011) and the Labot Fault (Fodor et al., 1998). A continuation into the Drau (Drava) Subfault System is expected. It shows a long-lasting history, with initial shear zones and faults in the Koralpe region during Cretaceous times. It was reactivated as right-lateral strike-slip faults during Miocene to Pliocene times and syn-tectonic basin formation of Fohnsdorf, Obdach and Lavant. Rates of 10-20 km horizontal (Fodor et al., 1998, Linzer et al, 2002 and references therein) and 2-5 km vertical (Kurz et al., 2011) displacement are described. According to Frisch et al., (2000) a displacement of the Periadriatic Fault System by 20 km is suggested.
Dieses etwa NNW-SSE-streichende ca. 150 km lange Störungssystem verläuft vom Pölstal (südlich Trieben) über Judenburg und Obdach ins Lavanttal und über Lavamünd (Labot) nach Drauburg (Dravograd) weiter ins Mislinja-Tal (SLO) und bis Slovenske Konjice (südlich des Pohorje-Gebirge), wo sie ins Sava-Sostanje-Donat-Störungssystem übergeht bzw. von diesem abgeschnitten wird. Sie setzt sich aus der Pöls- (Decker et al. 1994), Lavanttal-Störung (Linzer et al., 2002; Kurz et al., 2011) und Labot-Störung (Fodor et al., 1998) zusammen. Die Bewegungsphasen lassen sich in mehrere Zeitabschnitte untergliedern: So wird eine Initiierung entlang von Scherzonen und Störungen im Gebiet der Koralpe während der Oberkreide bis Paläogen diskutiert. Ihre Hauptprägung erfuhr sie im Miozän bis Pliozän mit dextral-seitenverschiebender Kinematik, Bildung/Einsenkung der miozänen Fohnsdorf-, Obdach-, Lavanttal-Becken und Versatzweiten von 10-18 km horizontal (Fodor et al., 1998, Linzer et al, 2002 und die darin aufgeführten Referenzen) und 2-5 km vertikal (Kurz et al., 2011) sowie ein Versatz des Periadriatische Lienament-Störungssystem von bis zu 20 km wird angenommen (Frisch et al., 2000).
Pöls-Lavanttal-Störungssystem
Pöls Fault
Pöls-Störung
The NNW-SSE trending fault along the valley of the Pöls is part of the Pöls-Lavantal Faultsystem and runs from Oberzeiring through St. Joahnn am Tauern to west of Hohentauern. A left-lateral displacement of 12 km is described (Decker et al., 1994).
Die NNW-SSE-streichende Störung entlang des Pölstales ist Teil des Pöls-Lavanttal-Störungssystems und verläuft von Oberzeiring durch St. Johann am Tauern bis westlich von Hohentauern. Ein sinistraler Versatz von 12 km wird angenommen (Decker et al., 1994).
Die NW-SE-streichende Störung entlang des Bretsteinbaches verläuft von Oberzeiring etwa 20 km in Richtung NW und wird dem Pöls-Lavanttal Störungssystem zugeordnet (Tollmann, 1986).
Bretstein Fault
Bretstein-Störung
The NW-SE trending fault running in the valley of the Bretsteinbach extends from Oberzeiring about 20 km in NW direction and belongs to the Pöls-Lavanttal Fault System (Tollmann, 1986).
Hirschegg Fault
Is a NE-SW trending fault near Hirschegg belonging to the Pöls-Lavanttal Fault System (Tollmann, 1986).
Ist eine NE-SW-streichende Störung bei Hirschegg und wird dem Pöls-Lavanttal Störungssystem zugeordnet (Tollmann, 1986).
Hirschegg-Störung
Obdach Fault
Is a NNE-SSW trending fault in the area of the village Obdach as part of the Pöls-Lavanttal Fault System (Tollmann, 1986).
Ist eine NNE-SSW-streichende Störung im Bereich von Obdach und Teil des Pöls-Lavanttal-STS (Tollmann, 1968).
Obdach-Störung
Labotski prelom
This subvertical NNE-SSW trending dextral strike slip fault runs in Austria parallel to the Lavant valley (Kurz et al., 2011; Linzer et al., 2002; Reischenbacher & Sachsenhoffer, 2013) and continues in NW-SE direction along the Drava and Mislinja valleys W of the Pohorje Mountains and then between Mislinja and Slovenske Konjice to the W of the Boč Mountain (e.g. Fodor et al., 1998; Atanackov et al., 2019). GPS measurements suggest the fault is recently active with an estimated average slip-rate of 0.5-1 mm/yr (Pavlovčič Prešeren et al., 2005). In Austria, seismic activity along the fault has been observed (XX)
Labot Fault
Lavanttal Fault
Lavanttal-Störung
Jadransko-Apulijski predgorski narivni sistem
Adriatic-Apulian Foreland Thrust System
The Adriatic-Apulian Foreland Thrust System comprises NW-SE striking, SW-vergent low-angle thrusts and reverse faults, extending from the Friuli plain across the northern Adriatic into the Istria peninsula (Placer, 2008; Placer et al., 2010). Also referred to as Istria-Friuli underthrust system (Placer et al., 2010).
Črnokalski nariv
Črni Kal Thrust
The Črni Kal Thrust is a 73 km long NW-SE striking, gently NE-dipping active thrust in extreme SW Slovenia, NW Croatia and the Gulf of Trieste (Atanackov et al., 2019). The surface trace runs from southern Friuli (NE Italy) in the NW to E Istria (NW Croatia). It is defined from geologic mapping and geophysical data (Pleničar et al., 1969; Celarc and Milanič, 2009; HGI, 2009; Placer et al., 2010; Busetti et al., 2010; Carulli, 2011). It is considered active, based on evidence from geophysical data (Romeo, 2009; Busetti et al., 2010).
Palmanova Thrust
Buzetski nariv
Buzet Thrust
Is a gently NE-dipping, 62 km long NW-SE striking thrust running across the Gulf of Trieste and SW Slovenia into NW Croatia (Atanackov et al., 2019). It runs from the Grado lagoon in the NW, across SW Slovenia into central Istria in NW Croatia (HGI, 2009; Placer et al., 2010; Busetti et al., 2010; Carulli, 2011). It is considered potentially active, based on its geometry with respect to the stress field and limited geodetic data (Rižnar et al., 2007).
Dinarski prelomni sistem
Dinaric Fault System
This fault system is composed of subparallel NW-SE striking, subvertical strike-slip faults running in the Slovenian part of the Southern Alps and the Northern Dinarides (Poljak et al., 2000; Vrabec in Fodor, 2006; Moulin et al., 2016, and references therein). The faults of this system cut older External Dinaric Thrust Belt and South Alpine Thrust and Fold Belt and have been dextrally active since the beginning of Pliocene. Some of the longest faults from this system are seismically active, e.g. the Ravne, Idrija, Predjama-Avče and Raša faults (e.g. Poljak et al., 2000; Kastelic et al., 2008; Vičič et al., 2019).
Idrija Fault System
Kranjski prelom
Kranj Fault
The fault runs in NW-SE direction along the southern rim of the Ljubljana Basin from Bled to Kranj (Poljak, 2007; Jamšek Rupnik, 2013). This is steeply NE-dipping dextral strike slip fault, which is considered as potentially still active in Quaternary times (Atanackov et al., 2019).
Planinsko-Podpreskin prelom
Planina-Podpreska Fault
This is a NW-SE striking and steeply SW-dipping dextral transpressive fault running along the Loški potok and Travljanska gora in mountainous terrain between Lož and Kočevje poljes (Atanackov et al., 2019, and references therein).
Rakitniški prelom
Rakitna Fault
This is a NW-SE striking and steeply NE-dipping dextral transpressive fault running from Horjul in NW across the Ljubljana Moor and further through the mountainous terrain, through Rakitna and Sodražica to the Ribnica Polje in SE. The fault is considered as potentially still active in Quaternary times (Atanackov et al., 2019; and references therein).
Idrija-Ampezzo prelomni podsistem
Idrija-Ampezzo Subfault System
About 200 km long system composed of steeply NE-dipping and approximately NW-SE-striking dextral strike-slip faults running through Friuli region in Italy along the Resia and Tagliamento valleys (Poli and Zanferrari, 2018) and in Slovenia from the Julian Alps through the Northern Dinarides along the Soča valley through Idrija and along several karst poljes in the SE part; Planina, Cerknica and Lož poljes (e.g. Poljak et al., 2000; Moulin et al., 2016). The system has been active in Pliocene and Quaternary.
Idrijski prelom
Idrija Fault
About 120 km long, NW-SE striking and steeply NE-dipping fault runs along the Soča Valley between Žaga and Most na Soči, then along several smaller valleys towards Idrija, further towards Logatec and then along the Planina, Cerknica and Lož poljes (Poljak, 2007; Atanackov et al., 2019, and references therein). The fault has been active as dextral strike-slip fault in Pliocene and Quaternary and is recently seismically active (Moulin et al., 2016; Atanackov et al., 2019; Vičič et al., 2019).
Mišjedolski prelom
Mišja dolina Fault
This is a NNW-SSE striking and subvertical dextral strike-slip fault running along the Gradaščica Valley, through the Ljubljana Moor to the Iška Village and continues through the mountainous terrain along the Mokrec Mountain and Mišja Valley towards Sodražica (Poljak, 2007; Atanackov et al., 2019; and references therein). Quaternary displacements along the fault were documented (Atanackov, 2013).
Raški prelom
Raša Fault
This 87 km long, NW-SE striking subvertical dextral strike slip fault runs from Goriška Brda on NW, across Vipava Valley, along the NE edge of the Kras plateau and through the Raša Valley, through Vremščica and Ilirska Bistrica in SE (Buser, 1968; Janež et al., 1997; Moulin et al., 2016; Jurkovšek, 2013; Placer and Jamšek, 2011; Atanackov et al., 2019). The fault has been active in Pliocene and Quaternary and is recently seismically active (Moulin et al., 2016; Vičič et al., 2019).
Divaški prelom
Divača Fault
The fault runs along the prominent scarp through the Kras plateau in Slovenia. This is NW-SE striking and steeply NE-dipping dextral strike slip fault, which is considered as probably still active in Quaternary times (Jurkovšek, 2013; Atanackov et al., 2019).
Dražgoški prelom
Dražgoše Fault
This is NW-SE striking and steeply NE-dipping dextral strike slip fault running from Pokljuka plateau in Slovenian Julian Alps, along the Jelovica plateau through Dražgoše, further SE along the Selška Sora Valley to the Kranj-Sora Polje (Poljak, 2007; Jamšek Rupnik, 2013; Atanackov et al., 2019). The fault is considered as probably still active in Quaternary times (Atanackov et al., 2019).
Topliški prelom
Toplice Fault
The Toplice fault is a SE-NW striking vertical dextral strike slip fault. The surface trace is 36 km long, from Senožeti in the NW to Žužemberk in the SE. Its trace is defined based on geologic mapping data (Mlakar, 1987; Buser, 1969, Premru, 1983). It is considered active based on seismicity (Atanackov et al., 2019).
Zagorski prelom
Zagorje Fault
This is a SE-NW striking vertical dextral strike slip fault with a 26 km surface trace. It runs from Trojane in the NW to Brunk in the SE (Buser, 1997; Placer, in prep., Celarc et al., 2009). It is considered probably active (Atanackov et al., 2019).
Hrastniški prelom
Hrastnik Fault
The Hrastnik fault is a SE-NW striking vertical dextral strike slip fault with a 26 km surface trace. It runs from Vrhe in the NW, to Zabukovje in the SE (Pleničar et al., 1976; Buser, 1977; Celarc et al., 2009; Placer, in prep.). It is considered probably active (Atanackov et al., 2019).
Želimeljsko-Ortneški prelom
Želimlje-Ortnek Fault
The fault runs from Ljubljana in NW, along the eastern rim of the Ljubljana Moor and then along the Želimeljščica Valley, across Velike Lašče, Ortnek and continues along the Ribnica and Kočevje poljes in SE (Poljak, 2007; Atanackov et al., 2019, and references therein). This NNW-SSE striking and steeply ENE dipping dextral strike-slip fault is considered as probably still active in Quaternary times (Atanackov et al., 2019).
Ravenski prelom
Ravne Fault
The Ravne fault is NW-SE striking and steeply NE-dipping dextral strike slip fault running through the mountainous terrain in the Slovenian part of the Julian Alps between Bovec and Cerkno (Atanackov et al., 2019, and references therein). The fault was the source of damaging 1998 Mw 5.6 and 2004 Mw 5.2 earthquakes (Kastelic et al., 2008, and references therein).
Dobrepoljski prelom
Dobrepolje Fault
NW-SE striking and steeply NE-dipping dextral strike slip fault running from the Ljubljana Moor to the SE along the Dobrepolje, Kočevska Mala gora in Poljanska Valley to the Stari trg ob Kolpi (Poljak, 2007; Atanackov et al., 2019, and references therein). The fault is considered as probably still active in Quaternary times (Atanackov et al., 2019).
Čepleški prelom
Čeplez Fault
This is a NW-SE striking, steeply NE-dipping dextral strike-slip fault running through the mountainous terrain between Cerkno and Smrečje near Rovte (Mlakar, 1982; Atanackov et al., 2019). The fault is considered as potentially still active in Quaternary times (Atanackov et al., 2019).
Žužemberški prelom
Žužemberk Fault
This is an active, 70 km long, NW-SE striking and steeply NE-dipping dextral strike-slip fault, running from Gameljne in the NW across the Ljubljana Polje, through Grosuplje and along the Krka Valley through Žužemberk and Dolenjske Toplice in SE (e.g. Poljak, 2007; Atanackov et al., 2019, and references therein).
Predjamski prelom
Predjama-Avče Fault
The fault runs in NW-SE direction from Kambreško, through Avče then across the Banjšice and Trnovski Gozd plateaus further SE through Col and then between Nanos and Hrušica plateaus to Postojna (Janež et al., 1997; Poljak, 2007). This is 75 km long, steeply NE-dipping dextral strike-slip fault, active in Pliocene and Quaternary (Moulin et al., 2016; Atanackov et al., 2019).
Predjama Fault
Stiški prelom
Stična Fault
The Stična fault is a SE-NW striking vertical dextral strike slip fault. It runs along a 26 km trace from Domžale in the NW to Dol pri Ljubljani in the SE. Its trace is defined based on geologic mapping data (Mlakar, 1987; Buser, 1969, Premru, 1983). It is considered probably active (Atanackov et al., 2019), however, no firm evidence of activity has been found.
Rabski prelomni sistem
Raba Fault System
The Raba Fault System is a set of Lower-Neogene WSW-ENE trending normal faults that separate the Burgenland swell in SE Austria from the Murska Sobota extensional block in NE Slovenia (Márton et al., 2002; Fodor et al., 2011). The Raba Fault System definition extends to neighbouring faults with related histories (e.g. formed in the same tectonic phase) and generally similar geometric and kinematic properties. The Raba Fault System is considered inactive.
Lovrenški prelom
Lovrenc Fault
The fault is based on geologic data (Mioč and Žnidarčič, 1978; Žnidarčič and Mioč, 1989; Maros et al., 2012) and geomorphic analysis. The 28 km long E-W trace runs from Ribnica na Pohorju in the W to Maribor in the E. The fault originated as a lower-Neogene normal fault, bounding the Ribnica half-graben and is inferred to be recently reactivated as a reverse fault. It is considered a potentially active fault, in favourable orientation with the current stress field and activity along the nearby Labot/Lavanttal fault (Atanackov et al., 2019), however, no evidence of activity has been found so far.
Južnoalpski narivni pas
South Alpine Thrust and Fold Belt
South Alpine Thrust and Fold Belt is part of the Eastern Southern Alps, located to the east of the N Giudicarie Line, originated by polyphase compressional evolution of Tertiary age (Castellarin & Cantelli, 2000). The Neogene shortening in the Adria-Eurasia collision zone produced top-to-the south thrusting of the Alps south of the Periadriatic Fault System. Thrusting began in the Middle Miocene and mostly ended by the Pliocene. W-E striking and south verging thrusts are positioned in the southern part of the Julian Alps (NW Slovenia), in the southern part of the Kamnik-Savinja Alps (central-N Slovenia) (Poljak, 2007; Placer, 2008).
Litijski nariv
Litija Thrust
This is a Dinaric thrust, folded in the Alpine direction (Placer, 2008). It is running from Medvode in the west to the Litija in the E (Poljak, 2007).
Litija Overthrust
Dolski nariv
Dole Thrust
Dole Thrust is positioned below the Litija Thrust and has according to the Placer (2008), the same genesis; it is a Dinaric thrust, folded in the Alpine direction. It is running in the E-W direction in the vicinity of Dolsko (Poljak, 2007).
Dole Nappe
Kumski nariv
Kum Thrust
Kum Thrust represents eastern continuation of the Dole Thrust (Placer, 2008) and has the same genesis. It is running in the E-W direction east from Kum, north from Sevnica and near Kozje (Poljak, 2007).
Kum Nappe
Furlanska prelomna domena
Friuli Fault Domain
This is a thrust and fold belt in the Southern Alps, composed of south-verging reverse faults. Seismically active reverse faults have a roughly E-W trend and turn southwest in the western part (e.g. Poli and Zanferrari, 2018).
Kobariški prelom
Kobarid Fault
Slovenian part of Kobarid Fault runs in approximately W-E direction between Breginj and Kobarid in the Julian Alps (Atanackov et al., 2019, and references therein). This is a N-dipping thrust, related to the Gemona Fault in Italy (Bressan et al., 2016). The fault is considered as potentially active through the Quaternary (Atanackov et al., 2019).
Gemona Thrust
Tolminski nariv
Tolmin Thrust
Podmelec Overthrust
E-W striking and gently N dipping thrust, part of the South Alpine Thrust and Fold Belt (Poljak, 2007; Placer, 2008), running from Breginj in the west under southern foothills of the Julian Alps to the Selce on east, where it continues as Selce Thrust.
Krnski nariv
Krn Thrust
E-W striking and gently N dipping thrust, part of the South Alpine Thrust and Fold Belt (Poljak, 2007; Placer, 2008), running from Bovec in the west under southern foothills of the Julian Alps.
Krn Overthrust
Jeloviški nariv
Jelovica Thrust
E-W striking and gently N dipping thrust, part of the South Alpine Thrust and Fold Belt (Poljak, 2007; Placer, 2008). This is probably eastern extension of the Krn Thrust. It is positioned along eastern foothills of the Jelovica Plateu near Kropa.
Jelovica Overthrust
Selški nariv
Selca Thrust
Part of the South Alpine Thrust and Fold Belt, originally E-W striking and gently N dipping, now it is partially overprinted with younger tectonic phases (Poljak, 2007; Placer, 2008). It is positioned in the vicinity of Škofja Loka.
Selca Overthrust
Zunanjedinarski narivni pas
External Dinaric Thrust and Fold Belt
The External Dinarides are built of thrust units, striking in the NW-SE direction with southwest vergence (Poljak, 2007; Placer, 2008; Placer et al., 2010). They were formed in the time from Upper Jurassic to Upper Eocene, and even to Lower Oligocene.
Snežniški nariv
Snežnik Thrust
The lowermost thrust of the External Dinaric Thrust Belt (Poljak, 2007; Placer, 2008; Placer et al., 2010) of the Eocene age. NW – SE striking and gently NE dipping, running from Razdrto in the NW, near Ilirska Bistrica and toward Rijeka (Croatia).
Snežnik Overthrust
Hrušiški nariv
Hrušica Thrust
The intermediate thrust of the External Dinaric Thrust Belt (Poljak, 2007; Placer, 2008; Placer et al., 2010) of the Eocene age. NW – SE striking and gently NE dipping, running from vicinity of Ajdovščina in the NW, Vipava, around foothills of the Nanos mountain and toward Postojna.
Hrušica
Trnovski nariv
Trnovo Thrust
The uppermost thrust of the External Dinaric Thrust Belt (Poljak, 2007; Placer, 2008; Placer et al., 2010) of the Eocene age. NW – SE striking and gently NE dipping, running from Nova Gorica, along the SW, S and E slopes of the Trnovo Plateau toward Idrija. It is dextrally displaced by strike-slip Predjama-Avče Fault.
Trnovo Overthrust
Zahodni Belokranjski nariv
Bela Krajina W Thrust
This is thrust of the External Dinaric Thrust Belt (Poljak, 2007; Placer, 2008; Placer et al., 2010) of the Eocene age. It is NW-SE striking and gently NE dipping thrust, running through Bela Krajina from Dobliče near Črnomelj on NW to Vinica on SE.
Periadriatisch-Mittelungarisches-Großstörungssystem
Periadriatic-Mid-Hungarian Large-scale Fault System
Periadriatsko-Srednjemadžarski veliki prelomni sistem
Insubric-Mid-Hungarian Large-scale Fault System
This ca. 1000 km long, approximately E-W and locally NE-SW trending Large-scale Fault System extends from Ivrea (IT) via the Veltlin Valley (Tonale Fault System) and the Sulztal until Cles. Here, it is displaced left-laterally by the Giudicarie Fault System. The eastern part starts in Sterzing (IT) and extends via the Eisack Valley, Pustertal (Pusteria), Gailtal and the Karawanks mountain range. There it splits into a northern and southern branch until the Lavant(Labot)-Mislinja Valley, where it splits again into several branches. The Lavanttal (Labot) Fault System displaces this Large-scale Fault System right-laterally. Finally, it continues eastward as the Middle Hungarian-Balaton Fault System (Fodor et al., 1998 and references therein). Deformation along this Large-scale Fault System can be subdivided into several phases: The potentially oldest deformation as NE-SW trending horst-and-graben structure from Permian to Lower Jurassic times is still under discussion (Pomella et al., 2012 and references therein). The first observed deformation is represented by Upper Cretaceous transpressive left-lateral shear zones (Müller et al., 2001). The main deformation phase with accompanying plutonic intrusions (Adamello, Bergell) is characterized by both, brittle and ductile, late Eocene-Miocene deformation with right-lateral movement. Recent deformation is reported from the eastern part (Handy et al., 2005 and references therein). Displacement rates are discussed controversially, reaching from at least 100 km of extension parallel to the orogen (Handy et al., 2005 and references therein) up to 500 km (Tari & Pamic, 1998 and discussion therein).
Dieses in etwa E-W (teilweise NE-SW)-streichende ca. 1000 km lange Großstörungssystem zieht sich von Ivrea (nördlich Turin) über das Veltlintal (Tonale-Linie) und das Sulztal bis nach Cles, wo es durch das Judikarien-Störungssystem sinistral versetzt wird. Bei Sterzing wiederbeginnend verläuft es über das Eisacktal, Pustertal, Gailtal und die Karawanken in einen Nord- und Südteil trennend bis zum Lavant-Mislinja-Tal, wo es sich in mehrere Arme auffächert und durch das Lavanttal-Störungssystem dextral versetzt wird. Anschließend setzt es sich nach Osten ins Mittelungarisch-Balaton-Störungssystem (Fodor et al., 1998 und die darin aufgeführten Referenzen) fort. Die Bewegungsphasen entlang dieses Großstörungssystems lassen sich in mehrere Zeitabschnitte untergliedern. Die Anlage als NE-SW-streichende vom Perm bis Lias aktive Horst und Grabenstruktur ist in Diskussion (Pomella et al., 2012 und die darin aufgeführten Referenzen). Die ersten nachgewiesenen Bewegungen werden durch oberkretazische Scherzonen mit sinistral transpressiver Kinematik repräsentiert (Müller et al., 2001). Die Hauptphase mit begleitenden plutonischen Intrusionen (Adamello, Bergell) zeigen duktile und spröde Deformation mit dextraler Kinematik vom späten Eozän bis Miozän. Rezente Bewegungen sind besonders aus den östlichen Anteilen beschrieben (Handy et al. 2005 und die darin aufgeführten Referenzen). Kontrovers sind die ermittelten Versatzweiten von mindestens 100 km orogen paralleler Extension (Handy et al. 2005 und die darin aufgeführten Referenzen) bis 500 km Versatz (Tari & Pamic 1998 und die darin aufgeführten Referenzen).
Srednjemadžarsko-Balatonski prelomni sistem
Mid-Hungarian-Balaton Fault System
Mittelungarisches-Balaton-Störungsystem
Orehovški prelom
Orehovec Fault
The Orehovec fault is a sinistral strike-slip fault in the NW part of the Gorjanci Mountains in SE Slovenia. The SW-NE running 28 km long fault trace runs from Semič in the SW to Orehovec in the NE (Bukovac et al., 1984). The fault dips vertically. It is considered probably active, based on geomorphic evidence and geologic mapping (Atanackov et al., 2019).
Donački prelom
Donat Fault
This dextral strike-slip fault runs along a 53 km long ENE-WSW trace from south of the Boč Mountain to Miklavž pri Ormožu (Aničić and Juriša, 1985; Maros et al., 2012). It is considered potentially active, being in a favourable geometric relationship with the current stress field and being part of the active Mid-Hungarian zone (Atanackov et al., 2019), however, no firm evidence of activity has been observed.
Haloški prelom
Haloze Fault
The Haloze fault is a 45 km long, steeply dipping N-vergent and E-W striking reverse fault, part of the Mid-Hungarian zone. The surface trace / projection of the fault runs from north of Boč Mountain to Ormož (Aničić and Juriša, 1985; Žnidarčič and Mioč, 1989; Mioč and Marković, 1998; Maros et al., 2012). It is considered potentially active, being in a favourable geometric relationship with the current stress field and being part of the active Mid-Hungarian zone (Atanackov et al., 2019), however, no firm evidence of activity has been observed.
Ljutomerski prelom
Ljutomer Fault
This blind reverse fault runs along a 28 km long E-W oriented surface trace projection from Savci in the west to the extreme E tip of Slovenia in the east (Mioč and Marković, 1998; Maros et al., 2012). It is a steeply dipping N-vergent blind fault, defined based on deep seismic reflection data (Atanackov, 2007). It is considered probably active, being in a favourable geometric relationship with the current stress field and being part of the active Mid-Hungarian zone (Atanackov et al., 2019). No conclusive evidence of activity has been found, however, geomorphic evidence in the associated Ormož-Selnica anticline suggests recent activity.
Periadriatski prelom
Periadriatic Fault System
Periadriatisches Störungssystem
This approximately 700 km long, E-W trending Fault System extends from Ivrea (IT) at its western margin via the Veltlin Valley (Tonale Fault System) and the Sulztal until Cles. Here, it is displaced left-laterally by the Giudicarie Fault System. The eastern part starts in Sterzing (IT) and runs via the Eisack Valley, Pustertal (Pusteria), Gailtal and the Karawanks Mountains towards the E. There it splits into a northern and southern branch until the Lavant (Labot)-Mislinja Valley, where it splits again into several branches. It is cut off by right-lateral movement along the Lavanttal (Labot) Fault System and continues to the East into the Middle-Hungarian-Balaton Fault System (Fodor et al., 1998 and references therein). It shows a long-lasting history with a main activity, accompanied by plutonic Intrusions (e.g. Pohorje), with right-lateral ductile and brittle movement during late Eocene to Miocene times. Recent activity along the fault is observed. Displacement rates of at least 100 km orogeny parallel extension is described (Handy et al. 2005 and references therein; Linzer et al. 2002 and references therein).
Dieses in etwa E-W - streichende ca. 700 km lange Störungssystem verläuft von Ivrea (nördlich Turin) über das Veltlintal (Tonale-Linie) und das Sulztal bis nach Cles, wo es durch das Judikarien-Störungssystem sinistral versetzt wird. Bei Sterzing wiederbeginnend verläuft es über das Eisacktal, Pustertal, Gailtal und die Karawanken in einen Nord- und Südteil trennend bis zum Lavant-Mislinja-Tal, wo sie sich in mehrere Arme auffächert und durch das Lavanttal- Störungssystem dextral versetzt wird. Anschließend setzt es sich nach Osten ins Mittelungarisch-Balaton- Störungssystem (Fodor et al., 1998 und die darin aufgeführten Referenzen) fort. Die Bewegungsphasen entlang dieses Störungssystem lassen sich in mehrere Zeitabschnitte untergliedern. Die Hauptphase mit begleitenden plutonischen Intrusionen (Pohorje) zeigt duktile und spröde Deformation mit dextraler Kinematik vom späten Eozän bis Miozän bis zu rezenten Bewegungen (Sprenger, 1996). Ermittelte Versatzweiten orogen paralleler Extension liegen bei mindestens 100 km (Handy et al. 2005 und die darin aufgeführten Referenzen; Linzer et al. 2002 und die darin aufgeführten Referenzen).
Periadriatic Fault
The Slovenian part of the Periadriatic Fault runs approximately in E-W direction through the northeastern part of the Kamnik-Savinja Alps and is cut by the Šoštanj Fault in the E. This is subvertical dextral transpressive fault, that was probably active also through the Quaternary (Fodor et al., 1998; Atanackov et al., 2019).
Periadriatic Line
Šoštanjski prelom
Šoštanj Fault
Approximately 90 km long, WNW-ESE striking subvertical dextral strike slip fault that runs through Šoštanj and along the southern rim of the Velenje Basin, through Dobrna towards Rogaška Slatina and further towards the E, where it enters Croatia (e.g. Poljak, 2007; Atanackov et al., 2019). The fault has been active also through Quaternary with an estimated slip-rate of 0.1-0.9 mm/yr (Atanackov et al., 2019, and references therein).
Meninsko-Vranski prelom
Menina-Vransko Fault
The ENE-WSW-striking an N-dipping reverse Menina-Vransko Fault runs along the southern edge of the Menina Mountain and the western rim of the Celje Basin (Fodor et al., 1998; Atanackov et al., 2019). The fault is considered as potentially active through the Quaternary (Atanackov et al., 2019).
Karavanški prelomni podsistem
The E-W trending fault is part of the Periadriatic Fault System with dextral-lateral kinematics in the Karavanks Mountains.
Die E-W-streichende Störung ist Teil des Periadriatischen Störungssystem mit dextral-seitenverscheibender Kinematik im Bereich der Karawanken (Polinski & Eisbacher, 1992).
Karavanke Subfault System
Karawanks Subfault System
Karawanken Subfault System
Karawanken-Teilstörungssystem
Severnokaravanški prelom
Diese hauptsächlich überschiebende Störung im Bereich der Karawanken ist Teil des Karawanken-Substörungssystems, das wiederum zum Periadriatischen Störungssystem gehört (Polinski & Eisbacher, 1992). In Österreich verläuft die E-W streichende, nach S einfallende Störung südlich der Drau vom Rabenberg via Unterloibl bis Zauchen/Suha. Der slovenische Teil der Störung verläuft zwischen Mežica und dem Slovenj-Gradec-Becken. Diese SSE-NNW-streichende, nach SSW einfallende Überschiebung wird als potentiell im Quartär aktiv angesehen (Nemes et al., 1997; Fodor et al., 1998; Atanackov et al., 2019).
Northern Karawanks Fault
This fault with mainly thrusting character within the Karawanks Mountains is part of the Karawanks Subfault System, which in turn is part of the Periadriatic Fault System (Polinski & Eisbacher, 1992). In Austria, the E-W trending and S-dipping fault runs south of and parallel to the Drau River, from the Rabenberg Mt. via the village of Unterloibl towards Zauchen/Suha. The Slovenian part of the Northern Karawanks Fault runs between Mežica and the Slovenj Gradec Basin. This SSE-NNW-striking and SSW-dipping thrust is considered as potentially active through the Quaternary (Nemes et al., 1997; Fodor et al., 1998; Atanackov et al., 2019).
Nördliche Karawanken-Störung
Feistritz-Störung
Feistritz Fault
The ENE-WSW trending fault in the Southern Alps runs from close to the Austrian-Slovenian border 5 km south of Bad Eisenkappel (AT) to Podljubelj (SLO), where it terminates at the Hochstuhl Fault.
Die ENE-WSW-streichende Störung der Südalpen verläuft nahe der österreichisch-slowenischen Grenze von 5 km südlich von Bad Eisenkappel (AT) bis nach Podljubelj (SLO), wo sie von der Hochstuhl-Störung abgeschnitten wird.
Karavanke Fault
Karavanks Fault
This E-W trending fault with right-lateral movement in the area of the Karawanken Mountains is part of the Periadriatic Fault System (Polinski & Eisbacher, 1992).
Diese E-W-streichende Störung mit dextral-seitenverscheibender Kinematik im Bereich der Karawanken ist Teil des Periadriatischen Störungssystem mit (Polinski & Eisbacher, 1992).
Karawanken-Störung
Karawanken Fault
Belsko-Savsko-Celjski prelomni podsistem
Fella-Sava-Celje Subfault System
This is an approximately W-E striking, 250 km long system consisting of the reverse Fella Fault and the dextral transpressive Sava and Celje faults (Placer, 1996; Fodor et al., 1998; Vrabec and Fodor, 2006; Jamšek Rupnik, 2013; Poli and Zanferrari, 2018). It runs from the Carnic Alps in Italy (Fella Fault), through the Upper Sava Valley in Julian Alps in Slovenia and along the northern rim of the Ljubljana Basin (Sava fault) and continues eastwards between the Kamnik-Savinja Alps and Sava Hills and along the southern rim of the Celje Basin (Celje Fault). The system has been active in Quaternary.
Savsko-Celjski prelom
Sava E - Celje Fault
The fault runs between the Kamnik-Savinja Alps and the Sava Hills in Slovenia and along the southern rim of the Celje Basin. This E-W striking steeply N-dipping dextral transpressive fault is considered active also through the Quaternary (Vrabec in Fodor, 2006; Atanackov et al., 2019).
Savski prelom
Sava W Fault
The fault runs through the Upper Sava Valley in the Julian Alps in Slovenia and along the northern rim of the Ljubljana Basin, where it separates the Kamnik-Savinja Alps from the Ljubljana Basin (Jamšek Rupnik, 2013; Atanackov et al., 2019). This is a WNW-ESE striking steeply NNE-dipping dextral transpressive fault, with documented Quaternary displacements (Jamšek Rupnik, 2013).
Sava Fault
Pustertal-Gailtal Subfault System
This approximately E-W trending Subfault System extends along the Puster and Gail Valleys (Pustertal and Gailtal, respectively) and are part of the Periadriatic Fault System. It shows a long-lasting history with right-lateral ductile and brittle movement during late Eocene to Miocene times. Recent activity along the fault is observed. (Handy et al, 2005; Mancktelow et al, 2001; Sprenger, 1996)
Pustertal-Gailtal-Teilstörungssystem
Dieses ca. E-W-streichende Teilstörungssystem verläuft entlang des Pustertals und Gailtals und ist Teil des Periadriatischen Störungssystem. Es zeigt eine duktile und spröde Deformation mit dextral-seitenverschiebender Kinematik vom Eozän bis ins Miozän. Rezente seismische Aktivität ist beschrieben. (Handy et al, 2005; Mancktelow et al, 2001; Sprenger, 1996)
Gailtal Fault
Gailtal-Stoerung
This approximately E-W trending fault along the valleys of the River Gail is part of the Pustertal-Gailtal Subfault System of the large-scale Periadriatic Fault System. It shows a long-lasting history with right-lateral ductile and brittle movement during late Eocene to Miocene times. Recent activity along the fault is observed. (Handy et al, 2005; Mancktelow et al, 2001; Sprenger, 1996)
Die in etwa E-W-streichende Störung entlang des Gailtals zählt zum Pustertal-Gailtal-Teilstörungssystem des Periadriatischen Störungssystems. Es zeigt eine duktile und spröde Deformation mit dextral-seitenverschiebender Kinematik vom Eozän bis ins Miozän. Rezente seismische Aktivität ist beschrieben. (Handy et al, 2005; Mancktelow et al, 2001; Sprenger, 1996)
Pusteria Fault
Pustertal-Störung
Linea della Pusteria
This approximately E-W trending Fault along the valley of the River Puster is part of the Pustertal-Gailtal Subfault System of the large-scale Periadriatic Fault System. It shows a long-lasting history with right-lateral ductile and brittle movement during late Eocene to Miocene times. Recent activity along the fault is observed. (Handy et al, 2005; Mancktelow et al, 2001; Sprenger, 1996)
Die in etwa E-W-streichende Störung entlang des Pustertals zählt zum Pustertal-Gailtal-Teilstörungssystem des Periadriatischen Störungssystems. Es zeigt eine duktile und spröde Deformation mit dextral-seitenverschiebender Kinematik vom Eozän bis ins Miozän. Rezente seismische Aktivität ist beschrieben. (Handy et al, 2005; Mancktelow et al, 2001; Sprenger, 1996)
Linea ad andamento SSE-NNO con cimenatica transpressiva destra.
Pustertal Fault
Nördliche Judikarien-Störung
Giudicarie North Line
Linea delle Giudicarie nord
NE-SW transfer zone acting first with a sinistral strike-slip displacement of some tens kms, then inverted as thrust with a western domain overthrusting the eastern one.
Linea di traferimento NE-SO che ha agito prima con un movimento trascorrente sinsitro di alcune decine di mk, quindi invertita a sovrascorrimento con il settore occidentale a sovrascorrere quello orientale. Https://doi.org/10.1016/j.tecto.2005.10.019
Canavese-Störung
Canavese Fault
Linea del Canavese
SW-NE trending lineament with dextral strike slip movement.
Linea ad andamento SO-NE con movimento trascorrente destro.
Tonale Fault
Tonale-Störung
Linea del Tonale
W-E trending lineament with dextral strike slip movement, up to 100 km.
Linea ad andamento O-E con movimento trascorrente destro fino a 100 km.
Insubrische Linie
This fault system demarcates the boundary between Africa and Europe plates. It is the original suture, potentially dating back to the Hercynian orogeny, which separates the S-verging Southalpine from the N-verging Penninic and Austroalpine domains. It is constituted, from west to east, by the SW-NE Canavese Line and the W-E Tonale Line (with important dextral strike slip movements (60-100 km along the Tonale Fault). The displacement continues along its eastern prolongation, the SW-NE N-Giudicarie Line, the NNW-SSE Pusteria and Gailtal Lines.
Insubric Fault System
Linea Insubrica
Questo sistema di faglie marca il limite tra le placche europea e africana; è una zona di sutura, potenzialmente riferibile già all'orogenesi ercinica, che separa il Sudalpino, vergente a sud, dai domini Pennidico e Austroalpino, con vergenza verso nord. Esso è costituito, da ovest verso est: dalla linea del Canavese, ad andamento SO-NE, e da quella del Tonale, ad andamento O-E, caratterizzate da una rilevante componente trascorrente destra del movimento (60-100 km lungo la linea del Tonale), dalla linea delle Giudicarie, ad andamento SO-NE, dalla linea della Pusteria e Gailtal, ad andamento NNO-SSE. Questo sistema di faglie è parte del lineamento regionale denominato Periadriatico.
Idrijski triasni prelomni snop
Idrija Triassic Fault Set
Idrija Triassic Fault Set is a system of predominately E-W striking Triassic (Ladinian) normal faults, related to the aborted continental rifting at the edge of the expanding Meliata Ocean (Mlakar & Čar, 2009, and references therein). Faulting led to formation of half-grabens, filled with thick succession of the clastic rocks, connected with volcanic activity and Hg mineralization of the famous Idrija mercury mine. Normal faults are cut by younger thrusts of the External Dinaric Thrust Belt or faults of the Dinaric Fault System.
Zavraški prelom
Zavratec Fault
E-W striking Triassic (Ladinian) normal – (aborted) rifting related – fault, E from the Idrija town (central-west Slovenia) (Mlakar & Čar, 2009, and references therein).
Ledinski prelom
Ledine Fault
E-W striking Triassic (Ladinian) normal – (aborted) rifting related – fault, N from the Idrija town (central-west Slovenia) (Mlakar & Čar, 2009, and references therein).
Ravenovški prelom
Ravenovo Fault
SSE-NNW striking Triassic (Ladinian) normal – (aborted) rifting related – fault, W from the Idrija town (central-west Slovenia) (Mlakar & Čar, 2009, and references therein).
Rudiščni prelom
Rudišče Fault
E-W striking Triassic (Ladinian) normal – (aborted) rifting related – fault, SE from the Idrija town (central-west Slovenia) (Mlakar & Čar, 2009, and references therein).
All named tectonic boundary objects that are located (at least partly) in Austria, are identified by an ID with the prefix „AT“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Instance of a tectonic boundary, as as they appear on the HIKE European fault database. They were published on the Geological Map of Austria at the scale of 1:1.000.000 of the Geological Survey of Austria.
Tectonic Boundary in Austria
Instanz einer Tektonischer Grenzfläche, wie sie in Datensätzen und Karten der Geologischen Bundesanstalt publiziert ist.
Tektonische Grenzfläche in Österreich
Görtschitztal Fault System
This ca. 50 km long, approximately NNW-SSE trending Fault System between the Gurktal and Sau Alps extends from the Neumarkt Sattel, following the Görtschitz Valley via Hüttenberg and Brückl to the Drau Valley. Its terminology and subdivision was in detail described by Fritsch (1963). It shows a significant vertical displacement with uplift of the E block during Eocene and Oligocene times indicated by deposits of the Gosau sediments in the Krappfeld. Proofs for right-lateral movement in the Miocene are described. (Frisch et al, 1998, 2003)
Dieses in etwa NNW-SSE-streichende ca. 50 km lange Störungssystem verläuft vom Neumarkter Sattel über Hüttenberg, das Görtschitztal zwischen Gurktaler Alpen und Saualpe über Brückl bis ins Drautal. Zur Nomenklatur und die Aufsplitterung in verschiedene Teiläste wurde von Fritsch (1963) beschrieben. Die Bewegungsphasen lassen sich in mehrere Zeitabschnitte untergliedern: Ein signifikanter vertikaler Versatz und Hebung des Ostteils, was mit einem eozänen bis oligozänen Einsenken der Gosauvorkommen des Krappfeldes in Verbindung stehen wird angenommen, welcher sich im Miozän als dextrale Seitenverschiebung fortsetzt. (Frisch et al, 1998, 2003)
Görtschitztal-Störungssystem
The NNE-SSW trending brittle fault with right-lateral movement in the Görtschitz Valley is part of the Görtschitztal Fault System (Fritsch, 1963).
Die NNW-SSE-streichende dextral-seitenverschiebende spröde Störung ist Teil des Görtschitztal-Störungssystem (Fritsch, 1963).
Görtschitztal Fault
Görtschitztal-Störung
The NNE-SSW trending fault from Glanegg to Althofen in the area of the Zollfeld (Carinthia) at the border to the Klagenfurt basin is part of the Görtschitztal Faultsystem (Kahler, 1953).
Die NNE-SSW-streichende Störung im Zollfeld (Kärnten) von Glanegg bis Althofen ist Teil des Görtschitztal-Störungssystems am Rand des Klagenfurter Beckens (Kahler, 1953).
Zollfeld Fault
Zollfeld-Störung
The NNE-SSW trending fault with right-lateral movement in the area of the town Griffen is part of the Görtschitztal Faultsystem and runs from about 4 km north of St. Oswald to Bleiburg (Kleinschmidt & Wurm, 1966; Seeger & Thiedig, 1983).
Die NNE-SSW-streichende Störung mit dextral-seitenverschiebender Kinematik ist Teil des Görtschitztal-Störungssystem und verläuft von 5 km nördlich von St. Oswald bis Bleiburg (Kleinschmidt & Wurm, 1966; Seeger & Thiedig, 1983).
Griffen Fault
Griffen-Störung
Male Karpaty Fault
This NE-SW trending fault is a part of the Vienna Basin Fault System (FS) at the eastern border of the Vienna Basin in the area of the Little Carpathian Mountains (Male Karpaty). It has normal faulting character. (Lenhardt et al., 2007; Nemcok et al., 1989)
Ist eine NE-SW-streichende Störung als Teil des Wien-Beckens Störungssystem (STS) am Ostrand des Wiener Beckens im Bereich der Kleinen Karpathen (Male Karpaty) mit initial abschiebender Kinematik. (Lenhardt et al., 2007; Nemcok et al., 1989)
Kleine Karpathen-Störung
Dieses grob N-S (teilweise NNE-SSW)-streichende ca. 250 km Großstörungssystem zieht vom Etschtal im Süden über Bozen bis Meran, wo es sich in mehrere Äste, über das Passeiertal bis Sterzing und die Sarntaler Alpen bis Mauls verzweigt, dann weiter nach Norden über den Brenner und das Silltal bis nach Innsbruck zum Inntal. Es setzt sich aus dem S und N-Judikarien- und Brenner-Silltal-Störungssystem zusammen und beinhaltet auch mehrere etwa parallel streichende (Teil)-Störungssysteme, wie das Jaufen-Passeier-Störungssystem (Viola et al., 2001), Meran-Mauls-Störungssystem (Viola et. al., 2001; Schmid et al., 2013), Fartleis-Pejo-Teilstörungssystem und das Naif-Völlan-Trento-Cles-Teilstörungssystem. Ihr signifikantes Erscheinungsbild ist der sinistrale Versatz des Canavese-Tonale-Periadriatisch-Mittelungarisches Großstörungssystem um 80 km (Pomella et al., 2011 und die darin angegebenen Referenzen). Eine Anlage bzw. Erhaltung von präexistierenden überschiebenden kretazischen und eozänen Scherzonen und dextralen Seitenverschiebungen ist beschrieben (Fügenschuh et al., 1997, Pomella et al., 2015). Ihre Hauptprägung dieses Großstörungssystem erfolgte bei der oligozänen-miozänen Intendierung der Adriatischen Mikroplatte nach Norden mit einer sinistral seitenverschiebenden Komponente und teilweise überschiebende Strukturen im südlichen Abschnitt. Aktivität bis in rezente Zeiten ist beobachtbar.
Giudicarie-Brenner-Silltal Large-scale Fault System
This ca. 250 km long, approximately N-S (and partly NNE-SSW) trending large-scale fault system extends from the Adige (Etsch) Valley at its southern end via Trento, Bolzano to Merano (IT) where it splits into several branches, along the Passeier Valley until Sterzing (IT) and along the Sarntal Mountains until Mauls. It continues towards the north via the Brenner and Sill Valleys until Innsbruck (AT). It includes several parallel trending (sub-)fault systems, like the Orobic Subfault System, the S-and N-Giudicarie Fault System, the Meran-Mauls Fault System (Viola et. al., 2001; Schmid et al., 2013), the Jaufen–Passeier Fault System, the Fartleis-Pejo Subfault System (Viola et al., 2001), the Naif-Völlan-Trento–Cles Subfault System and the Brenner-Silltal Fault System. The major characteristic of this large-scale fault system is the left-lateral displacement of the Canavese-Tonale-Periadraric-Midhungarian Large-scale Fault System for about 80 km (Pomella et al., 2011 and reference therein). Proofs of pre-existing thrusting and right-lateral strike-slip faulting during Cretaceous and Eocene times are observed. (Fügenschuh et al., 1997; Pomella et al, 2015). The main deformation phase of this large-scale fault system occurred during the Oligocene-Miocene northward movement of the Adriatic microplate. This is combined with left-lateral strike-slip and thrusting components at its southern part. Recent activity along the fault is observed.
Giudicarie-Brenner-Silltal-Großstörungssystem
fault (IT-0051)
fault (IT-4189)
fault (IT-0048)
This ca. 45 km long, approximately N-S-trending Fault System extends from Sterzing (IT) to the Brenner Pass following the Sill Valley to the Inn Valley, where it is cut by the Engadin-Inntal Fault System. It includes the Brenner and Silltal subfault systems and parallel trending faults and shear zones. Proofs of pre-existing nappe boundaries with top E and W kinematics during Cretaceous, reactivated from the late Oligocene to Miocene as W-dipping normal fault with top W sense of shear and left-lateral strike-slip faults are observed (Fügenschuh et al., 1997). Displacement rates are discussed controversially, depending on the vertical displacement reaching from 10 up to 27,5 km and the dip-angles of the normal fault, indicating a total displacement of 14 to 70 km respectively. (Fügenschuh et al., 1997 and references therein; Rosenberg & Garcia, 2011)
Dieses grob N-S-streichende ca. 45 km lange Störungssystem zieht von Sterzing über den Brennerpass und das Silltal bis ins Inntal, wo es vom Engadin-Inntal-Störungssystem abgeschnitten wird. Es beinhaltet das Brenner- und das Silltal-Teilstörungssystem mit parallel verlaufenden Störungen und Scherzonen. Seine Anlage als kreidezeitliche Deckengrenze mit EW-Kinematik und eine spät-Oligozäne bis Miozäne Reaktivierung als W-einfallende Abschiebung mit top W-gerichteter Kinematik sowie sinistral seitenverschiebender Kinematik wurden beschrieben. Ein Vertikalversatz von 10-27,5 km und dip-slip Versatzweiten von 14-70 km werden diskutiert. (Fügenschuh et al., 1997 und die darin aufgeführten Referenzen; Rosenberg & Garcia, 2011)
Brenner-Silltal Fault System
Brenner-Silltal-Störungssystem
This N-S trending fault system in the area of the Brenner Pass is part of the Brenner-Silltal Fault System. Normal faulting is described (Fügenschuh et al., 2000).
Diese N-S-streichende Störung im Bereich des Brennerpasses ist Teil des Brenner-Silltal-Störungssystem. Abschiebende Kinematik ist beschrieben (Fügenschuh et al., 2000).
Brenner Subfault System
Brenner-Teilstoerungssystem
This N-S trending fault in the area of the Brenner Pass is part of the Brenner-Silltal Fault System. Steep brittle normal faulting is described (Fügenschuh et al., 2000).
Diese N-S-streichende Störung im Silltal (W des Brennerpasses) ist Teil des Brenner-Silltal-Störungssystem. Steilstehende spröde abschiebende Kinematik ist beschrieben (Fügenschuh et al., 2000).
Brenner Fault
Brenner-Stoerung
The N-S trending ductile shear zone in the area of the Brenner Pass is part of the Brenner-Silltal Fault System. Gently dipping ductile normal faulting is described (Fügenschuh et al., 2000).
Diese N-S-streichende Störung im Silltal (W des Brennerpasses) ist Teil des Brenner-Silltal-Störungssystem. Flach einfallende duktile abschiebende Kinematik ist beschrieben (Fügenschuh et al., 2000).
Brenner Shearzone
Brenner-Scherzone
This N-S trending fault in the area of the Brenner Pass is part of the Brenner-Silltal Fault System. Normal faulting is described (Fügenschuh et al., 2000).
Diese N-S-streichende Störung im Silltal (W des Brennerpasses) ist Teil des Brenner-Silltal-Störungssystem. Abschiebende Kinematik ist beschrieben (Fügenschuh et al., 2000).
Silltal Fault
Silltal-Stoerung
This N-S trending fault in the area of Mt. Portjoch (W of the Brenner Pass) is part of the Brenner-Silltal Fault System. Normal faulting is described (Fügenschuh et al., 2000).
Die N-S-streichende Störung im Bereich des Portjoch (W des Brennerpasses) ist Teil des Brenner-Silltal-Störungssystem. Abschiebende Kinematik ist beschrieben (Fügenschuh et al., 2000).
Portjoch Fault
Portjoch-Störung
fault (IT-0030)
Diendorf-Boskovice-Cebin Large-scale Fault System
This ca. 230 km long, approximately NNE-SSW (and partly NE-SW) trending Large-scale Fault System extends from Cebin (CZ), following the Boskovice furrow and the graben of Zöbing to Diendorf in the south. It includes the Diendorf-Boskovice Fault System and Cebin Fault, showing a long-lasting and multiphase history. Parallel trending structures and conjugated shear zones and faults are correlated with this Large-scale Fault System. Proofs of NE-SW-trending left-lateral strike-slip partly ductile, mylonitic shear zones during upper Carboniferous and Permian times are observed in the Diendorf Subfault System. To the north it continues to horst-graben structures filled with upper Carboniferous to Permian sediments (Rostinsky et al., 2001). The deformation continuous left-lateral strike-slip faulting during Miocene and recent times. (Lenhardt et al., 2007; Rostinsky et al., 2013)
Dieses in etwa NNE-SSW – streichende (teilweise NE-SW), ca. 230 km lange Großstörungssystem zieht sich von Cebin (CZ), entlang dem Boskovice-Graben, dann von Miozänen Sedimenten bedeckt bis zum Graben von Zöbing und weiter bis Diendorf. Es setzt sich aus dem Diendorf-Boskovice-Störungssystem und der Cebin-Störung zusammen und zeigt eine langandauernde und multiphase Entwicklung. Parallel streichende Strukturen und konjugierte Scherzonen und Störungen werden mit diesem Großstörungssystem assoziiert. Duktile mylonitische Scherzonen mit sinistral seitenverschiebender Kinematik des oberen Karbons bis Perms (Rostinsky et al., 2013) sind vorwiegend entlang des Diendorf-Teilstörungssystem beschrieben und setzt sich nach Norden in von oberkarbonen-permischen Sedimenten verfüllte Horst und Grabenstruktur fort (Rostinsky et al., 2001). Diese wird durch spröde Störungen mit sinistral seitenverschiebender Kinematik überprägt, welche bis in rezente Zeit beobachtbar sind. (Lenhardt et al., 2007; Rostinsky et al., 2013)
Diendorf-Boskovice-Cebin-Großstörungssystem
Diendorf-Boskovice Fault System
This ca. 200 km long, approximately NNE-SSW (and partly NE-SW) trending Fault System extends from the Boskovice furrow and the graben of Zöbing to Diendorf in the south. It includes the Diendorf and Boskovice Subfault System, showing a long-lasting and multiphase history. Proofs of NE-SW-trending left-lateral strike-slip partly ductile, mylonitic shear zones during upper Carboniferous and Permian times are observed in the Diendorf Subfault System. To the north it continues to horst-graben structures filled with upper Carboniferous to Permian sediments (Rostinsky et al., 2001). The deformation continuous left-lateral strike-slip faulting during Miocene and recent times. (Lenhardt et al., 2007; Rostinsky et al., 2013)
Dieses in etwa NNE-SSW - streichende (teilweise NE-SW) ca. 200 km lange Großstörungssystem zieht vom Boskovice-Graben bis zum Graben von Zöbing und weiter bis Diendorf. Es setzt sich aus dem Diendorf- und Boskovice-Teilstörungssystemen zusammen und zeigt eine langandauernde und multiphase Entwicklung. Duktile mylonitische Scherzonen mit sinistral seitenverschiebender Kinematik des oberen Karbons bis Perms (Rostinsky et al., 2013) sind vorwiegend entlang des Diendorf-Teilstörungssystem beschrieben und setzt sich nach Norden in von oberkarbonen-permischen Sedimenten verfüllte Horst und Grabenstruktur fort (Rostinsky et al., 2001). Diese wird durch spröde Störungen mit sinistral seitenverschiebender Kinematik überprägt, welche bis in rezente Zeit beobachtbar sind. (Lenhardt et al., 2007; Rostinsky et al., 2013)
Diendorf-Boskovice-Störungssystem
Diendorf Subfault System
This subfault system contains the Austrian part of the Diendorf-Boskovice fault system and consists of several parallel NNE-SSW trending faults.
Dieses Substörungssystem umfasst den österreichischen Teil des Diendorf-Boskovice-Störungssystems und setzt sich aus verschiedenen parallel zueinander laufenden, haupsächlich NNE-SSE streichenden Störungen zusammen.
Diendorf-Teilstörungssystem
The N-S striking normal fault runs in the valley of the River Kamp from Fernitz to Kammern, where it terminates at a subfault of the Diendorf-Boskovice Fault System. Top to the west faulting was active during the Eggenburgian.
Die N-S-streichende Abschiebung verläuft im Kamptal von Fernitz bis Kammern, wo sie an einer Teilstörung des Diendorf-Boskovice-Störunggssystems endet. Die Bewegungsrichtung des Hangendblocks ging im Eggenburgium gegen Westen.
Mörtersdorf Fault
Mörtersdorf-Störung
This NE-SW trending fault extends from Waitzendorf towards Retz and Znojmo (CZ). It runs parallel to and northwest of the Diendorf Fault. The Waitzendorf Fault delimits the Thaya Batolith towards the East. Cataclastic fault rocks indicate mainly brittle deformation along the fault.
Diese NE-SW-streichende Störung verläuft zwischen Waitzendorf, Retz und Znojmo (CZ, Znaim), nordwestlich und parallel zur Diendorf-Störung. Diese Störung begrenzt den Thaya-Batholith nach Osten hin. Kataklase Störungsgesteine weisen auf eine hauptsächlich spröde Deformation hin.
Waitzendorf Fault
Waitzendorf-Störung
Emsrütti Fault
NE-SW striking normal fault between the towns of Götzis, Hohenems and Dornbirn that offsets the eastern margin of the Rhine Valley. (Oberhauser, 1991, Zerlauth, 2014)
NE-SW streichende Abschiebung, die zwischen Götzis, Hohenems und Dornbirn den Ostrand des Rheintales abschiebend versetzt. (Oberhauser, 1991; Zerlauth, 2014)
Emsrütti-Störung
Ragga-Teuchl Fault System
This ca. 35 km long, approximately NW-SE, partly NNE-SSW trending Fault System extends from Baldramsdorf in the Möll Valley to Teuchl and the Ragga-Alm. Here, it is displaced left-laterally by the Wöllatratten Fault. Then it extends from Stall up to Sagritz. It includes parallel trending shear zones and faults (Hoke, 1990). Proofs of pre-existing nappe boundaries during Cretaceous times which were reactivated as ductile shear zones and faults with right-lateral strike-slip movement during Oligocene times are observed (Ilickovic & Schuster, 2014).
Dieses etwa WNW-ESE-streichende ca. 35 km lange Störungssystem zieht sich von Baldramsdorf im Mölltal über Teuchl und die Ragga-Alm. Im oberen Mölltal wird sie sinistral von der Wöllatratten-Störung versetzt und verläuft von Stall weiter bis Sagritz. Es beinhaltet parallel verlaufenden Störungen und Scherzonen (Hoke, 1990). Es wurde als Deckengrenze in der Oberkreide angelegt und als duktile Scherzonen und spröde Störungen mit dextral seitenverschiebender Kinematik im Oligozän reaktiviert (Ilickovic, 2014).
Ragga-Teuchl-Störungssystem
Ragga-Teuchl Fault
The Ragga-Teuchl fault represents the brittle part of the Ragga-Teuchl Fault System and shows right-lateral movement. (Hoke, 1990; Ilickovic & Schuster, 2014)
Die Ragga-Teuchl-Störung repräsentiert den spröden Anteil des Ragga-Teuchl-Störungssystems mit spröder dextral seitenverschiebender Kinematik. (Hoke, 1990; Ilickovic & Schuster, 2014)
Ragga-Teuchl-Störung
The NE-SW striking and SE-dipping fault runs from Grosshöflein via Eisenstadt along the southeastern side of the Leitha Mountains towards Parndorf. The main deformation phase shows normal faulting character. (Tollmann, 1986)
Die NE-SW streichende, nach SE einfallende Störung verläuft von Großhöflein über Eisenstadt südöstlich vom Leithagebirge bis nach Parndorf. Die Hauptdeformation hat abschiebenden Charakter. (Tollmann, 1986)
Eisenstadt-Störung
Eisenstadt Fault
Gallneukirchen Fault
The NW-SE striking fault runs from Gallneukirchen via Mauthausen to Strengberg into the Molasse subsurface. It forms the SW margin of the Gallneukirchen Basin with top-to-the-NE normal movement. (Kröll et al., 2001; Seiberl et al., 1996)
Die NW-SE streichende Störung verläuft von Gallneukirchen über Mauthausen nach Strengberg in den Molasseuntergrund. Sie formt die SW-Grenze des Gallneukirchen-Beckens, wobei das Hangende gegen NE abgeschoben wurde. (Kröll et al., 2001; Seiberl et al., 1996)
Gallneukirchen-Störung
Formarin Fault
This NW-SE striking fault runs SW of the Rote Wand mountain from the Laguzbach Valley to Lake Formarin. (Tollmann, 1986).
Diese NW-SE streichende Störung verläuft südwestlich der Roten Wand vom Laguzbachtal zum Formarinsee. (Tollmann, 1986)
Formarin-Störung
NCA E-W Fault Set
This fault set of E-W trending faults within the Northern Calcareous Alps includes the Ebner Fault, Königsberg Fault, and Spullersee Fault amongst other similar orientated faults with same kinematics. These faults were probably generated during Oligocene-Early Miocene times as reverse faults. During Late Miocene N-S extension compression, they might have been reactivated as normal faults. (Peresson & Decker, 1997a, b)
Dieses Störungsset von E-W-streichenden Störungen in den Nördlichen Kalkalpen (NKA) beinhaltet die Ebner-, Königsberg-, Spullersee- und weitere ähnlich orientierte Störungen mir derselben Kinematik. Diese Störungen entwickelten sich seit dem Oligozän bis frühem Miozän als Überschiebungen und wurden während des späten Miozän als Abschiebungen reaktiviert. (Peresson & Decker, 1997a, b)
NKA-Störungsset (E-W)
Grünalmkogel Fault
The NE-SW striking fault runs from the Outer Weissenbach Valley at the Grünalmkogel moutain (Höllengebirge moutains) to the Langbathseen. (Tollmann, 1986)
Die NE-SW streichende Störung verläuft vom Tal des Äußeren Weißenbach am Grünalmkogel (Höllengebirge) vorbei zu den Langbathseen. (Tollmann, 1986)
Grünalmkogel-Störung
Ebner Fault
Is an E-W-trending brittle thrust fault in the western Northern Calcareous Alps (NCA). (Eisbacher & Brandtner, 1995, 1996)
Ist eine E-W-streichende spröde Störung mit überschiebender Kinematik in den westlichen Nördlichen Kalkalpen (NKA). (Eisbacher & Brandtner, 1995, 1996)
Ebner-Störung
Korneuburg Fault System
Korneuburg-Teilstörungssystem
This subfault system consists all faults related to the subsidence of the Korneuburg Basin NW of Vienna. It includes the Schliefberg and the Helfens Fault.
Dieses Teilstörungssystem beinhaltet alle Störungen, die im Zusammenhang mit der Einsenkung des Korneuburger Beckens im NW von Wien im Zusammenhang stehen, z.B. die Schliefberg- und Helfens-Störung.
Schliefberg Fault
The normal fault dips with more than 60° to ESE and limits the Korneuburg basin towards the WNW. The hanging wall in the E is offset by 800 m. (Wessely, 2006)
Die mit über 60° nach ESE einfallende Abschiebung begrenzt das Korneuburger Becken nach WNW hin ab. Das Hangende im E wird um 800 m versetzt. (Wessely, 2006)
Schliefberg-Störung
Drautal-Zwischenbergen-Wöllatratten Fault System
This ca. 60 long, NE-SW trending Fault System extends from Sillian, following the Drau Valley to Lienz. Here, it is displaced dextral-laterally by the Iseltal Fault System. The eastern part starts in Zwischenbergen, following the upper Möll Valley to Wöllatratten and Flattach. Itself it displaces the Ragga-Teuchl Fault System and includes parallel trending faults and shear zones. Proofs of pre-existing nappe boundaries during Cretaceous times, reactivated as left-lateral strike-slip faults during Miocene times are observed. (Ilickovic & Schuster, 2014; Probst et al, 2003)
Dieses NE-SW -streichende ca. 60 km lange Störungssystem zieht sich von Sillian, das Drautal entlang bis Lienz wo es durch das Iseltal-Störungssystem dextral versetzt wird und dann über Zwischenbergen das obere Mölltal bis Wöllatratten und Flattach folgt. Es versetzt das Ragga-Teuchl- Störungssystem und beinhaltet parallel verlaufende Störungen und Scherzonen, welche als kreidezeitliche Deckengrenze angelegt und als sinistral seitenverschiebende Scherzonen und Störungen im Oligozän und Miozän reaktiviert wurden. (Ilickovic & Schuster, 2014; Probst et al, 2003)
Drautal-Zwischenbergen-Wöllatratten-Störungssystem
The ENE-WSW trending brittle fault along the Drau Valley, from Sillian to Lienz, with left-lateral movement was active during the Miocene (Probst et al., 2003).
Die NE-SW-streichende spröde Störung entlang des Drautales, von Sillian nach Lienz, mit sinistral-seitenverschiebender Kinematik war im Miozän aktiv (Probst et al., 2003).
Drautal Fault
Drautal-Störung
The ENE-WSW trending brittle fault of the Drautal-Zwischenbergen-Wöllatratten Fault System was reactivated as left-lateral strike-slip fault during the Oligocene and Miocene (Probst et al, 2003).
Die NE-SW-streichende spröde Störung des Drautal-Zwischenbergen-Wöllatratten-Störungssystemes wurde als sinistral seitenverschiebende Scherzonen und Störungen im Oligozän und Miozän reaktiviert wurden (Probst et al, 2003).
Zwischenbergen-Wöllatratten Fault
Zwischenbergen-Wöllatratten-Störung
Csapod Fault
The NNE-SSW trending fault runs from Tadten and Parnhagen via Fertöszentmiklós (HUN) east of Csapod to Bö (HUN). It dips steeply towards the ESE and has been deformed as a normal fault. The main deformation phase occurred presumably during Eggenburgian and Sarmatian. (Csaszar, G., 2000)
Die NNE-SSW streichende Störung verläuft von Tadten und Parnhagen über Fertöszentmiklós (HUN) östlich von Csapod bis nach Bö (HUN). Sie fällt steil nach ESE ein und hat abschiebenden Bewegungscharakter. Die Hauptbewegungsphase war vermutlich zwischen Eggenburgium und Sarmatium. (Csaszar, G., 2000)
Csapod-Störung
Iseltal Fault System
This ca. 90 km long, approximately NW-SE trending Fault System extends from Matrei in Osttirol, following the Isel Valley to Oberdrauburg, continuing to St. Georgen im Gitschtal and Görtschach. It displaces the Drautal-Zwischenbergen-Wöllatratten Fault System and includes structures trending parallel to the Isel Valley. Proofs for right-lateral ductile (northern parts) and brittle movement during Miocene times with displacement rates of approximately 15-20 km are described. (Linzer et al., 2002)
Dieses in etwa NW-SE-streichende ca. 90 km lange Störungssystem zieht von Matrei im Osttirol über das Iseltal entlang bis Oberdrauburg, weiter über St. Georgen im Gitschtal bis Görtschach. Es versetzt das Drautal-Zwischenbergen-Wöllatratten- Störungssystem und beinhaltet parallel zum Iseltal verlaufenden Störungen, welche während des Miozän als Störungen und Scherzonen (nördliche Anteile) mit dextral seitenverschiebender Kinematik aktiv waren. Versatzweiten von 15-20 km werden beschrieben. (Linzer et al., 2002)
Iseltal-Störungssystem
This approximately NW-SE trending fault is the part of the Iseltal Fault System and runs extends from Matrei in Osttirol, following the Isel Valley to Lienz and continues parallel to the Drau Valley until Görtschach. Proofs for right-lateral ductile (northern parts) and brittle movement during Miocene times with displacement rates of approximately 15-20 km are described. (Linzer et al., 2002)
Diese NW-SE-streichende Störung ist Teil des Iseltal-Störungssystem und zieht sich von Matrei im Osttirol über das Iseltal entlang bis Lienz, und weiter im Drautal bis Görtschach. Dextral seitenverschiebender Kinematik und Versatzweiten von 15-20 km werden für das Miozän beschrieben. (Linzer et al., 2002)
Iseltal Fault
Iseltal-Störung
Anger-Piregg Fault
The steeply inclined Arlui Fault extends from Reith via Birkfeld and Anger towards Gleisdorf in an arch-shape. Most probably, the fault has a polyphase deformation history, where the eastern block has been moved downwards. (Schuster & Ilickovic, 2015)
Die steilstehende Störung verläuft bogenförmig von Reith über Birkfeld und Anger bis Gleisdorf. Vermutlich wurde die Störung polyphas bewegt, wobei auf jeden Fall der Ostblock abgesenkt wurde. (Schuster & Ilickovic, 2015)
Anger-Piregg-Störung
Inntal Thrust
This fault is a roughly E-W trending thrust fault. It was active during middle to late Cretaceous times and was reactivated as right-lateral strike-slip fault during Miocene. (Eisbacher & Brandtner, 1996; Ortner et al., 2006)
Diese Überschiebung is eine ungefähr E-W-streichende spröde Überschiebung mit top-to-the-WNW/NW-gerichteter Kinematik, welche während der mittleren bis oberen Kreide angelegt wurde und während des Miozäns als dextrale Seitenverschiebung reaktiviert wurde. (Eisbacher & Brandtner, 1996; Ortner et al., 2006)
Inntal-Überschiebung
Engadin-Inntal-Innsbruck-Salzburg-Amstetten Large-scale Fault System
This ca. 400 km long, approximately WSW-ENE (and partly SW-NE) trending Large-scale Fault System extends from Bregaglia Valley(north of the Bergell massive), following the Inn Valley to Nauders, Pfunds, Imst and Telfs. At Telfs, it is dextrally offset by the Telfs Subfault System. The eastern part strikes from Innsbruck to Wörgl and Kufstein continuing over Salzburg to Amstetten. It includes the Engadin-Inntal and Innsbruck-Salzburg-Amstetten fault systems and shows a long-lasting deformation history with significant displacement. Proofs of thrusting and normal faulting during Cretaceous and Paleogene times are observed (Froitzheim et al., 1997), continuing with left-lateral strike-slip faulting during upper Oligocene to recent times. Displacement reaches up to around 17 km of normal faulting and 74-135 km of left-lateral displacement. (Egger, 1997; Froitzheim et al., 1997; Linzer et al., 2002 and references therein)
Dieses ca. WSW-ESE - streichende ca. 400 km lange Großstörungssystem zieht vom Bregaglia-Tal (nördlich des Bergell-Massivs) über das Inntal bis Nauders, Pfunds, Imst und Telfs. Am Telfs-Teilstörungssystem wird das Großstörungssystem dextral versetzt und verläuft dann von Innsbruck über Wörgl bis Kufstein und dann über Salzburg nach Amstetten. Es beinhaltet das Engadin-Inntal- sowie Innsbruck-Salzburg-Amstetten-Störungssystem und zeigt eine lang andauernde Bewegungsgeschichte mit beträchtlichen Versatzweiten. So wird eine frühe kreidezeitliche bis paläogene Initiierung im Ostteil mit über- und abschiebender Kinematik beschrieben, welche sich vom obersten Oligozän bis rezent mit sinistral seitenverschiebender Kinematik fortsetzt. Eine horizontale Gesamtversatzweite von 74-135 km kann angenommen werden. (Egger, 1997; Froitzheim et al., 1997; Linzer et al., 2002 und die darin aufgeführten Referenzen)
Engadin-Inntal-Innsbruck-Salzburg-Amstetten-Großstörungssystem
Engadin-Inntal Fault System
This ca. 225 km long, approximately SW-NE trending Fault System extends from Bregaglia Valley (north of the Bergell massive), following the Inn Valley to Nauders, Pfunds, Imst and Telfs. Here, it is displaced right-laterally by the Telfs Subfault System. The eastern part starts in Innsbruck to Wörgl and Kufstein. It includes subfault systems along the Engadin and Inn valleys and parallel trending structures such as the Schlinig, Gallo and Arlui shear zones. It shows a long-lasting history and was initiated as ductile nappe boundaries and shear zones with E-dipping, top-to-the-W-directed thrusting and top-to-the-ESE-directed normal faults during Cretaceous and Paleogene times. During the Oligocene it was reactivated along shear zones with top WNW kinematics (e.g. Engadin and Schlinig shear zones). Left-lateral brittle strike-slip faults are active from the upper Oligocene to the Miocene, indicated by sediment deposits in the Inn Valley (Froitzheim et al, 1997; Ortner et al., 2006). Displacement rates can be summarized, reaching around 17 km of normal faulting and 31-75 km of left-lateral displacement. (Froitzheim et al., 1997; Linzer et al., 2002 and references therein)
Dieses in etwa NE-SW - streichende ca. 225 km Störungssystem zieht vom Bregaglia-Tal (nördlich des Bergell-Massivs) über das Inntal bis Nauders, Pfunds, Imst und Tels. Es wird am Telfs-Teilstörungssystem dextral versetzt und verläuft dann von Innsbruck das Inntal weiter über Wörgl bis Kufstein. Es beinhaltet die Engadin- und Inntal-Teilstörungssysteme sowie parallel verlaufende Strukturen, wie die Schlinig-, Gallo- und Arlui-Scherzonen. Die Bewegungsphasen lassen sich in mehrere Zeitabschnitte untergliedern: So wird eine Initiierung als duktile Deckengrenzen und Scherzonen mit W-gerichteten Überschiebungen und nach E-einfallende, top-to-the-ESE-Abschiebungen während der Oberkreide bis Paläogen, mit einer überschiebenden Reaktivierung im Oligozän entlang der Engadin-Scherzone beschrieben. Ihre spröde Hauptprägung erfuhr sie im späten Oligozän bis Miozän mit sinistral seitenverschiebender Kinematik und Sedimentation im Inntal. Auch rezente seismische Aktivität ist bekannt (Froitzheim et al, 1997; Ortner et al., 2006). Ermittelte Versatzweiten zeigen ca. 17 km abschiebende Werte, sinistral seitenverschiebende Versatzweiten für das Engadin-Teilstörungssystem von 3-20 km und für das Inntal-Teilstörungssystem von 31-75 km. (Linzer et al., 2002 und die darin aufgeführten Referenzen)
Engadin-Inntal-Störungssystem
Schlinig Subfault System
This approximately 20 km long N-S striking subfault system runs between the Reschen Pass (Passo die Resia) and the area of the Vinschgau (Venosta Valley). The subfault system displaces the Ötztal nappe base by approximately 17 km (Froizheim et al., 1997).
Diese ca. 20 km lange N-S streichende Teiltörungssystem verläuft zwischen dem Reschenpass und dem Vinschgau und ist Teil des Engadin-Innsbruck-Störungssystemes. Das Substörungssystem versetzt die Ötztalbasisüberschiebung um ca. 17 km (Froizheim et al. 1997).
Schlinig-Teilstörungssystem
Schlinig Fault
The fault trace on the map describes a concave line towards the W (Trümpy, 1980) that extends from the Reschen Pass (Passo di Resia) to the Vinschgau (Venosta Valley). Froizheim et al. (1997) postulates that the Schlinig Fault, together with its southern continuation, the Gallo Fault, was generated as Late Cretaceous fault with top-to-the-SE shear sense.
Der Ausbiss der Schlining-Störung in der Karte beschreibt eine nach W hin konkave Linie (Trümpy, 1980), die sich vom Reschenpass bis zum Vinschgau hinzieht. Froizheim et al. (1997) postuliert die Schlinig-Störung zusammen mit ihrer südlichen Fortsetzung, der Gallo-Störung, als spätkretazische Abschiebung mit top-to-the-SE Schersinn.
Schlinig-Störung
Engadin Subfault System
This ca. 155 km long, approximately NE-SW trending fault system extends from Bregaglia Valley (North of the Bergell Massive), following the Inn Valley to Nauders, Pfunds, Imst and Tels. It includes faults along the Engadin Valley and parallel trending structures such as the Schlinig, Gallo, and Arlui shear zones. It shows a long-lasting deformation history and was initiated as ductile nappe boundaries and shear zones with E-dipping, top-to-the-W-directed thrusting and top-to-the-ESE-directed normal faults during Cretaceous and Paleogene times. During the Oligocene, it was reactivated along shear zones with top-to-the-WNW kinematics (e.g. Engadin and Schlinig shear zones). Left-lateral brittle strike-slip faults were active from the Upper Oligocene to the Miocene (Froitzheim et al, 1997). Total displacement amounts up to around 17 km normal faulting and 3-20 km left-lateral displacement. (Froitzheim et al., 1997; Linzer et al., 2002 and references therein)
Dieses in etwa NE-SW - streichende ca. 155 km lange Teilstörungssystem zieht vom Bregaglia-Tal (nördlich des Bergell-Massivs) über das Inntal bis Nauders – Pfunds –Imst bis Telfs. Es beinhaltet entlang und parallel des Engadin- Gebietes verlaufende Scherzonen und Störungen, wie die Schlinig-, Gallo und Arlui-Scherzonen. Eine Initiierung als duktile Deckengrenzen und Scherzone mit W-gerichteten Überschiebungen und Richtung E-einfallende top-ESE-Abschiebungen während der Oberkreide bis Paläogen, mit einer überschiebenden Reaktivierung im Oligozän ist beschrieben (Froitzheim et al., 1997). Ihre spröde Hauptprägung erfuhr sie im späten Oligozän bis Miozän mit sinistral seitenverschiebender Kinematik. Versatzweiten von ca. 17 km abschiebender Komponente und von 3-20 km sinistral seitenverschiebender Versatzweiten werden angenommen. (Froitzheim et al., 1997; Linzer et al., 2002 und die darin aufgeführten Referenzen)
Engadin-Teilstörungssystem
Gallo Fault
Inntal Subfault System
This ca. 170 km long, approximately SW-NE trending subfault system extends from Innsbruck, following the Inn Valley to Wörgl and Kufstein and then to Salzburg and Thalgau. It includes faults and shearzones along the Inn Valley and parallel trending structures. Left-lateral brittle strike-slip faults are active from the Upper Oligocene to the Miocene, indicated by sediment deposits described in the Inn Valley (Froitzheim et al, 1997; Ortner et al., 2006). Seismic activity has been observed along the Inn Valley. Total displacement reaches up to around 17 km normal faulting and 31-75 km left-lateral displacement. (Froitzheim et al., 1997; Linzer et al., 2002 and references therein)
Dieses in etwa NE-SW - streichende ca. 170 km lange Teilstörungssystem läuft das Inntal entlang von Innsbruck-Wörgl bis Kufstein und weiter über Salzburg bis Thalgau. Es beinhaltet entlang und parallel des Inntals verlaufende Störungen und Scherzonen. Ihre spröde Hauptprägung erfuhr sie im späten Oligozän bis Miozän mit sinistral seitenverschiebender Kinematik und Sedimentation im Inntal. Auch rezente seismische Aktivität ist bekannt. Es wurden Versatzweiten von 31-75 km ermittelt. (Froitzheim et al., 1997; Linzer et al., 2002 und die darin aufgeführten Referenzen)
Inntal-Teilstörungssystem
Die WSW-ENE-streichende spröde Störung ist Teil des Inntal-Teilstörungssystems. (Froitzheim et al., 1997; Linzer et al., 2002 und die darin aufgeführten Referenzen)
The WSW-ENE trending brittle fault is part of the of the Inntal Subfault System. (Froitzheim et al., 1997; Linzer et al., 2002 and references therein)
Inntal Fault
Inntal-Stoerung
The WSW-ENE trending shearzone containing the ductile part of the Inntal Subfault System, extends north of the Inn Valley over more than 80 km from south of Obergilben to north of Innsbruck and Hall/Tirol. (Froitzheim et al., 1997; Linzer et al., 2002 and references therein)
Die WSW-ENE-streichende und 10-20 km breite duktile Scherzone, die Teil des Inntal-Teilstörungssystems ist, erstreckt sich nördlich des Inntales über mehr als 80 km von südlich von Obergilben bis nördlich von Innsbruck und Hall in Tirol. (Froitzheim et al., 1997; Linzer et al., 2002 und die darin aufgeführten Referenzen)
Inntal Shear zone
Inntal-Scherzone
Innsbruck-Salzburg-Amstetten Fault System
The term Innsbruck-Salzburg-Amstetten Fault System (ISAM) was first mentioned by Egger (1997). He describes a mainly sinistral strike-slip fault system between Innsbruck, Salzburg and Amstetten which has offset the southern edge of the Northern Calcareous Alps by at least 40 km. The fault system runs parallel to the Inntal Shear Zone between Innsbruck and Kufstein. Between Salzburg and the Lake Mondsee, the fault runs along the northern rim of the Northern Calcareous Alps and runs between the lakes Mondsee and Attersee within the Flysch zone north of Hochplett. East of Lake Attersee, Egger (1997) describes two fault branches belonging to the ISAM. The Pettenbach Fault and a related fault in the south running from northern rim of the Ultrahelvetic Units from Gschliefgraben (Lake Traunsee) via the village of Untergrünburg (Steyrtal) towards Amstetten. In addition, all sinistral fault branches are kinematically linked to ISAM, which emerge from the ISAM and thereby offset the Rhenodanubian Flyschzone. (Egger, 1997)
Der Begriff Innsbruck-Salzburg-Amstetten-Störungssystem (ISAM) wurde von Egger (1997) zum ersten Mal erwähnt. Er beschreibt damit ein hauptsächlich sinistrales Blattverschiebungssystem zwischen Innsbruck, Salzburg und Amstetten, das den Kalkalpensüdrand um mindestens 40 km versetzt hat. Zwischen Innsbruck und Kufstein verläuft das Störungssystem parallel zur Inntalscherzone (bzw. entspricht der Inntalstörung). Zwischen Salzburg und dem Mondsee entspricht der Verlauf der Nordbegrenzung der Kalkalpen und verläuft zwischen Mond- und Attersee innerhalb der Flyschzone nördlich von Hochplett. Östlich vom Attersee werden von Egger (1997) zwei zur Innsbruck-Salzburg-Amstetten-Störungssystem gehörige Störungsäste beschrieben, die Pettenbach-Störung sowie ein südlich davon verlaufender Störungsast, der am Nordrand des Ultrahelvetikums von Gschliefgraben (Traunsee) über Untergrünburg (Steyrtal) nach Amstetten verläuft. Kinematisch verlinkt zur Innsbruck-Salzburg-Amstetten-Störungssystem sind zusätzlich alle sinistralen Störungsäste, die aus dieser abbiegen und dabei die Rhenodanubische Flyschzone versetzen. (Egger, 1997)
Innsbruck-Salzburg-Amstetten-Störungssystem
Mur-Mürz-Wiener-Becken-Vah-Großstörungssystem
Dieses ca. 400 km lange Großstörungssystem beinhaltet von S nach N das Mur-Mürz-Störungssystem, das Wiener Becken-Störungssystem sowie das Vah-Störungssystem (Decker et al., 2005) und ist kinematisch mit Überschiebungen in den äußeren Karpaten in Galizien (POL) verbunden. Es besteht hauptsächlich aus ENE-WSW-streichenden sinistralen Seitenverschiebungen und NNE-SSW-streichenden Abschiebungen. Seine Hauptphase war während des Miozäns als Folge der Ost-Bewegung der Ostalpen (Ratschbacher et al. 1991, Linzer et al., 2002). Versatzweiten von bis zu 40 km entlang des Abschnittes Mur-Mürz-Wiener Becken wurden ermittelt (Linzer et al., 2002). Erste Untersuchungen zu Erdbeben von Gutdeusch & Aric (1988) entlang der sogenannten Mur-Mürz-Wiener Becken-Zilina seismologische Zone deuten auf rezente seismische Aktivität hin.
Mur-Mürz-Vienna Basin-Vah Large-scale Fault System
From S to N, this ca. 400 km long Large-scale Fault System includes the Mur-Mürz Fault System, Vienna Basin Fault System, and the Vah Fault System (Decker et al., 2005) and seems to be kinematically linked to thrust faults in the outer Carpathians in Polish Galicia. This large-scale fault system consists mostly of ENE-WSW trending left-lateral strike-slip and NNE-SSW trending normal faulting. Onset of faulting along the entire large-scale fault system started in the Miocene as consequence of eastward extrusion of the Central Eastern Alps (Ratschbacher et al. 1991, Linzer et al., 2002). In total, Miocene offset in the Mur-Mürz-Vienna Basin area has been estimated to up to 40 km (Linzer et al., 2002). Earthquakes have been observed for the first time along the so-called Mur-Mürz-Vienna Basin-Zilina seismogenic zone by Gutdeusch & Aric (1988) proving recent activity of the large-scale fault system.
Mur-Mürz Fault System
The ca. 130 km long, approximately ENE-WSW trending fault system extends from Judenburg along the Mur and Mürz Valleys and builds the southern border of the Vienna Basin close to Gloggnitz (Frisch et al., 2002). The fault system consists mostly of left-lateral strike-slip faults, but includes also small pull-apart basins. Based on sedimentary deposits in the pull-apart basins, left-lateral deformation started in the Karpatian (Linzer et al., 2002). Miocene offset reaches up to 40 km. (Linzer et al., 2002)
Dieses ca. 130 km lange, ungefähr ENE-WSW-streichende Störungssystem verläuft von Judenburg, entlang des Mur- und Mürztales und bildet den Südrand des Wiener Beckens nahe Gloggnitz (Frisch et al, 2002). Es zeigt vorwiegend sinistral seitenverschiebende Kinematik mit der Bildung kleinerer Pull-Apart-Becken. Anhand sedimentärer Ablagerungen belegt, startet die Entwicklung im Karpatium, mit Versatzweiten bis zu 40 km. (Linzer et al., 2002)
Mur-Mürz-Störungssystem
Mur-Störung
This approximately ENE-WSW trending fault is part of the Mur-Mürz Fault System. It extends along the river Mur and shows left-lateral movement (Linzer et al., 2002; Tollmann, 1986). Recent seismic activity has been recorded along the fault (Reinecker & Lenhardt, 1999).
Die ungefähr ENE-WSW-streichende Störung ist teil des Mur-Mürz-Störungssystems. Sie erstreckt sich entlang des Murtales mit sinistral-seitenverschiebender Kinematik. (Linzer et al., 2002; Tollmann, 1986). Rezente seismische Aktivität ist beschrieben (Reinecker & Lenhardt, 1999).
Mur Fault
Mürz Fault
This approximately ENE-WSW trending fault extends along the valley of the river Mürz and shows left-lateral movement. (Linzer et al., 2002; Tollmann, 1986)
Es ist eine ungefähr ENE-WSW-streichende Störung entlang des Mürztales mit sinistral-seitenverschiebender Kinematik. (Linzer et al., 2002; Tollmann, 1986)
Mürz-Störung
Wiener-Becken-Störungssystem
Vienna Basin Fault System
The almost 200 km long, NNE-SSW trending, rhombohedral Vienna Basin consists of mostly NE-SW striking oblique left-lateral strike-slip faults at its eastern margin and NNE-SSW trending listric normal faults compensating E-W extension (Decker, 1996). It extends from Gloggnitz at its southern end via the recent flood plain of the River Danube between Vienna and Hainburg at its widest point towards Zilina in the North. Formation of the Vienna Basin Fault System started due to pull-apart subsidence during the Badenian at around 16 Ma and lasted until 9 - 8 Ma (Decker, 1996; Peresson & Decker, 1997; Hölzel et al., 2010). Quaternary reactivation is indicated by dissected Pleistocene terraces and Quaternary basins (Decker et al., 2005, Beidinger & Decker, 2011).
Dieses ca. 200 km lange, NNE-SSW-streichende Störungssystem beinhaltet alle Störungen und Strukturen des rhomboedrischen Wiener Pull-Apart-Beckens mit vorwiegend NE-SW-streichenden sinistralen Seitenverschiebungen an seinem Ostrand und NNE-SSW-streichende listrische Abschiebungen als Folge seiner E-W-Extension (Decker, 1996). Es zieht von Gloggnitz, seinem Südende, über die Donau zwischen Wien und Hainburg bis Zilina, an seinem Nordende. Es entstand als Pull-Apart-Becken während des Badenium (ca. 16 Ma) bis ins obere Miozän (9-8 Ma; Decker, 1996, Peresson & Decker, 1997; Hölzel et al., 2010). Quartäre Reaktivierungen der Störungen werden durch pleistozäne Terassenbildungen und quartäre Beckenbildungen dokumentiert (Decker et al., 2005, Beidinger & Decker, 2011).
Markgrafneusiedl Fault
The NE-SW, partly N-S trending, steeply E-dipping normal fault in the central part of the Vienna Basin runs from Fischamend via Wittau to Markgrafneusiedl. Between Markgrafneusiedl and Gänserndorf, it forms the eastern margin of the Pleistocene Gänserndorf terrace (Beidinger & Decker, 2011; Schopper, 1992; Wessely, 2000).
Die NE-SW, teilweise N-S-streichende, steil nach E einfallende Störung mit abschiebender Kinematik verläuft im zentralen Wiener Becken von Fischamend via Wittau nach Markgrafneusiedl. Zwischen Markgrafneusiedl und Gänserndorf bildet sie die östliche Begrenzung der pleistozänen Gänserndorfterrasse (Beidinger & Decker, 2011; Schopper, 1992; Wessely, 2000).
Markgrafneusiedl-Störung
This NNW-SSE trending, steeply E-dipping normal fault in the western part of the Vienna Basin running from Ebreichsdorf via Leopoldsdorf towards the City of Vienna. The Leopoldsdorf Fault crosses Vienna from Oberlaa via Schwedenplatz towards Strebersdorf (Küpper, 1968; Plachy, 1981; Beidinger & Decker, 2011).
Diese NNW-SSE-streichende, steil nach E einfallende Störung mit abschiebender Kinematik verläuft im westlichen Wiener Becken von Ebreichsdorf via Leopoldsdort nach Wien. Im Wiener Stadtgebiet lässt sie sich von Oberlaa über den Schwedenplatz bis nach Strebersdorf verfolgen (Küpper, 1968; Plachy, 1981; Beidinger & Decker, 2011).
Leopoldsdorf Fault
Leopoldsdorf-Störung
Schrattenberg Fault
This ENE-WSW trending normal fault splits from the Poysbrunn Fault at Hörersdorf and runs via Poysdorf to Schrattenberg and Valtice at the Austrian-Czech border (Schopper, 1992; Kovac et al., 2004).
Diese ENE-SSW-streichende Störung mit abschiebender Kinematik spaltet sich bei Hörersdorf von der Poysbrunn-Störung nach Osten ab und verläuft via Poysdorf bis nach Schrattenberg bzw. Valtice an der österreichisch-tschechischen Grenze (Schopper, 1992; Kovac et al., 2004).
Schrattenberg-Störung
Bisamberg Fault
It is a NNE-SSW trending brittle normal fault in the northwestern Vienna basin active since the Miocene (Beidinger & Decker, 2011 and references therein).
Es ist eine NNE-SSW-streichende Störung im nordwestlichen Wiener Becken mit abschiebender Kinematik welche seit dem Miozän aktiv ist (Beidinger & Decker, 2011 und die darin aufgeführten Referenzen).
Bisamberg-Störung
Pirawarth-Hochleiten Subfault System
It is a NE-SW trending normal fault in the northern part of the Vienna Basin (Wessely, 2006).
Es ist eine NE-SW-streichende Störung mit abschiebender Kinematik im nördlichen Wiener Becken (Wessely, 2006).
Pirawarth-Hochleiten-Teilstörungssystem
Kronberg Fault
This NE-SW striking and steeply SW dipping fault runs from Münichsthal to the North of Kronberg, parallel to the Putzing Fault (Grill, 1968). The normal offset is between 30 to 70 m.
Diese NE-SW streichende und steil nach SW einfallende Störung verläuft von Münichsthal bis nördlich von Kronberg parallel zur Putzing-Störung (Grill, 1968). Der abschiebende Versatz beträgt zwischen 30 und 70 m.
Kronberg-Störung
Putzing Fault
This NE-SW striking and steeply SW dipping fault is the southern end of the Pirawarth-Hochleiten Subfault System. It runs from Königsbrunn to Putzing, where it is displaced right-laterally for approximately 900 m by a E-W striking fault. It then continues until Riedenthal and is cut of there by a NW-SE striking fault (Grill, 1968). The normal offset is at least 150 m.
Diese NE-SW streichende und steil nach SW einfallende Störung bildet das südliche Ende des Pirawarth-Hochleiten-Teilstörungssystems. Sie verläuft von Königsbrunn bis Putzing, wo sie durch eine E-W verlaufende Störung um ca. 900 m rechtslateral versetzt wird. Sie verläuft dann weiter nach Norden bis Riedenthal, wo sie durch eine NW-SE streichende Störung abgeschnitten wird (Grill, 1968). Die Sprunghöhe beträgt mindestens 150 m.
Putzing-Störung
Dieses NW-SE streichende Teilstörungssystem erstreckt sich von Wagram an der Donau (AT) im SW via Lassee und Marchegg nach Zohor (SK). Es zeigt die Struktur einer negativen Blumenstruktur und entspricht dem von Beidinger & Decker (2011) beschriebenen Lassee-Segment
Lassee Subfault System
This NE-SW trending subfault system extends from Wagram an der Donau (Austria) in the SW via Lassee and Marchegg to Zohor (Slovakia). It has the structure of a negative flower structure and corresponds to the Lassee segment described by Beidinger & Decker (2011)
Lassee-Teilstörungssystem
This NE-SW trending fault is the main fault of the Lassee subfault system at depth, where all the fault strands reachting at the surface are rooting. It is mainly a strike slipe fault with a normal fault component (Beidinger & Decker, 2011).
Lassee Fault
Diese NE-SW-streichende Störung ist die Hauptstörung des Lassee-Teilstörungssystems, in dem alle an der Oberfläche sichtbaren Störungsäste in der Tiefe zusammenlaufen. Ihre hauptsächliche Kinematik ist sinistral seitenverschiebend mit einer bedeutenden abschiebenden Komponente (Beidinger & Decker, 2011).
Lassee-Störung
Steinberg Fault
This NNE-SSW striking and steeply ESE dipping fault runs from Gross-Schweinbarth via Zistersdorf and Neusiedl an der Zaya until north of Breclav (CZ; Kovac, 2004). The eastern hanging wall was offest by 5 km of normal faulting during the Miocene. During the Quaternary, this fault was probably reactivated together with other faults in the Vienna Basin. (Decker et al., 2005, Beidinger & Decker, 2011)
Diese NNE-SSW streichende, steil nach ESE einfallende Störung verläuft von Groß-Schweinbarth über Zistersdorf, Neusiedl an der Zaya bis nördlich von Breclav (CZ; Kovac, 2004). Der E-Block wurde während des Miozäns um rund 5 km abgeschoben. Im Quartär wurde die Störung vermutlich zeitgleich mit anderen Störungen im Wiener Becken abschiebend reaktiviert. (Decker et al., 2005; Beidinger & Decker, 2011)
Steinberg-Störung
Engelhartstetten Fault
It is a NE-SW trending fault at the eastern border of the Vienna Basin (Wessely, 2000).
Es ist eine NE-SW-streichende Störung am Ostrand des Wiener Beckens (Wessely, 2000).
Engelhartstetten-Störung
Poysbrunn Fault
This NNE-SSW trending normal fault is the northwestern margin of the Vienna Basin (Grill, 1968; Wessely, 2006). West of Poysbrunn, the fault runs from Olgersdorf via Falkenstein to Drasenhofen. In Hörersdorf, the Schrattenberg Fault splits from the Poysbrunn Fault.
Diese NNE-SSW-streichende Störung mit abschiebender Kinematik bildet die nordwestliche Begrenzung des Wiener Beckens (Grill, 1968). Sie verläuft westlich von Poysbrunn von Olgersdorf über Falkenstein bis Drasenhofen. Bei Hörersdorf vereint sie sich mit der Schrattenber-Störung (Wessely, 2006).
Falkenstein Fault
Falkensteiner Bruch, Falkenstein-Störung
Poysbrunn-Störung
Nussdorf-Störung
It is a NNE-SSW trending normal fault in the northwestern part of the Vienna Basin (Küpper, 1968).
Es ist eine NNE-SSW-streichende Störung im nordwestlichen Wiener Becken mit abschiebender Kinematik (Küpper, 1968).
Nussdorf Fault
Matzen Subfault System
It is a NE-SW trending normal fault in the Vienna Basin. (Schopper, 1992; Wessely, 2000)
Es ist eine NE-SW-streichende Störung im Wiener Becken mit abschiebender Kinematik. (Schopper, 1992; Wessely, 2000)
Matzen-Teilstörungssystem
This subfault system includes all faults related to the opening of the Mitterndorf Basin, the southernmost subbasin of the Vienna Basin. The Pottendorf Fault is part of this subfault system. Its extent corresponds to the extent of the Mitterndorf-Schwadorf segment described by Beidinger & Decker (2011).
Dieses Teilstörungssystem beinhaltet alle Störungen, die mit der Öffnung des Mitterndorf-Beckens im Süden des Wiener Beckens in Zusammenhang stehen. Die Pottendorf-Störung wird diesem Teilstörungssystem zugerechnet. Das Teilstörungssystem entspricht in der Ausdehnung dem Mitterndorf-Schwadorf-Segment von Beidinger & Decker (2011).
Mitterndorf Subfault System
Mitterndorf-Teilstörungssystem
Pottendorf Fault
This NE-SW trending normal fault is located at the southern part of the Vienna Basin. (Lenhardt et al., 2007; Schopper, 1992; Wessely, 1984, 2000)
Es ist eine NE-SW-streichende Störung mit abschiebender Kinematik im südlichen Wiener Becken. (Lenhardt et al., 2007; Schopper, 1992; Wessely, 1984, 2000)
Pottendorf-Störung
Aderklaa-Bockfliess-Teilstörungssystem
Aderklaa-Bockfliess Subfault System
This NNE-SSW striking and steeply dipping subfault system consists of several en-echelon faults running from Groß-Enzersdorf via Breitenlee, Aderklaa, Deutsch-Wagram, and Bockfließ to the south of Gross-Schweinbarth (Wessely, 2006). While the northern faults are parallel to the NNE-SSW striking main fault, the southern faults run NW-SE. The western block has been shifted downward during Miocene before it was reactivated in the Quaternary period. (Decker et al., 2005, Weissl et al., 2016)
Dieses NNE-SSW streichende, hauptsächlich steil nach WNW einfallende Teilstörungssystem besteht aus mehreren en-echelon angeordneten Störungen, die von Groß-Enzersdorf über Breitenlee, Aderklaa, Deutsch-Wagram und Bockfließ bis südlich von Groß-Schweinbarth verlaufen (Wessely, 2006) . Während die nördlichen Störungen parallel zur NNE-SSW streichenden Hauptstörung verlaufen, streichen die südlichen Störungen in NW-SE-Richtung. Der W-Block wurde während des Miozäns abgeschoben. Im Quartär wurde die Störung wiederum abschiebend reaktiviert. (Decker et al., 2005, Weissl et al., 2016)
Aderklaa-Bockfliess Fault
This NNE-SSW striking fault is the main fault of the Aderklaa-Bockfließ subfault system. It is the eastern margin of the Gänserndorf terrace and runs from Aderklaa via Deutsch-Wagram and Bockfließ to the south of Gross-Schweinbarth (Wessely, 2006).
Diese NNE-SSW streichende Störung ist die Hauptstörung des Aderklaa-Bockfliess-Teilstörungssystems. Sie bildet die Ostkante der Gänserndorf-Terrasse und verläuft von Aderklaa über Deutsch-Wagram und Bockfließ bis südlich von Groß-Schweinbarth (Wessely, 2006)
Aderklaa-Bockfliess-Störung
Pfahl Fault System
This NW-SE striking, steep to NE dipping fault system runs from the northeastern edge of the Bavarian Forest (D) through the Czech Republic and runs from Schwarzenberg (A) via Haslach an der Mühl to Rodl, where it is cut off from the Rodl fault system south of Obernaukirchen. The ductile major event, similar to the Rodl fault system, is applied to the late Variscian event, predominantly with a dextral direction of movement. It is considered that during Miocene a brittle reactivation with the same kinematics went on. (Brandmayr et al., 1997; Büttner, 2007; Siebel et al., 2005)
Dieses NW-SE streichende, steil nach NE einfallende Störungssystem zieht sich vom nördöstlichen Rand des Bayrischen Waldes durch die Tschechische Republik und verläuft ab Schwarzenberg (A) über Haslach an der Mühl bis zur Rodl, wo sie südlich von Obernaukirchen vom Rodl-Störungssystem abgeschnitten wird. Die duktile Hauptbewegungsphase wird, analog zum Rodl-Störungssystem, auf das Spätvariszikum gelegt, mit hauptsächlich dextraler Bewegungsrichtung. Von einer spröden miozänen Reaktivierung mit selber Bewegungskinematik wird ebenfalls ausgegangen. (Brandmayr et al., 1997; Büttner, 2007; Siebel et al., 2005)
Pfahl-Störungssystem
Ostergunten Fault System
It is a system setting up of several NNE-SSW striking, parallel running sinistral strike-slip faults with normal fault component on the east side of the Kanisfluh-Aniklinale, which extend from Buchboden (Großes Walsertal) via Schönbach-Vorsäße and Sibratsgfäll to Balderschwang (Bavaria, D). All together, the eastern block subsides approximately 600 m. The Ultrahelvetic Unit is offset by about 3 km. (Zerlauth et al., 2014)
Ein System aus mehreren NNE-SSW streichenden, parallel verlaufenden sinistralen Blattverschiebungen mit abschiebenden Komponente an der Ostseite der Kanisfluh-Aniklinale, die sich von Buchboden (Großes Walsertal) über Schönbach-Vorsäße und Sibratsgfäll nach Balderschwang (Bayern, D) hinziehen. Insgesamt kann von ca. 600 m Absenkung des östlichen Blocks ausgegangen werden. Das Ultrahelvetikum wird um ca. 3 km sinistral versetzt. (Zerlauth et al., 2014)
Ostergunten-Störungssystem
Palten-Liesing Fault System
This ca. 65 km long, approximately WNW-ESE trending Fault System extends from Lienz, following the Palten and Liesing Valleys to the village of St. Michael in der Obersteiermark in the Mur Valley. It includes the Palten and Liesing Fault Systems and shows right-lateral strike-slip movement during Miocene times. Total displacement of 8 km is assumed. (Kurz et al., 2011; Linzer et al., 2002; Metz, 1978)
Dieses in etwa WNW-ESE-streichende ca. 65 km lange Störungssystem verläuft von Liezen, über das Paltental und Liesingtal bis ins Murtal (St. Michael in der Obersteiermark). Sie setzt sich aus der Palten- und Liesing-Störung zusammen und zeigt dextral-seitenverschiebende Kinematik im Miozän. Ein Versatz von 8 km wird angenommen. (Kurz et al., 2011; Linzer et al., 2002; Metz, 1978)
Palten-Liesing-Störungssystem
Trofaiach Fault
It is an E-W trending fault along the northern part of the basin of Trofaiach and shows left-lateral movement. The belonging to the Mur-Mürz Fault System is discussed as well as its continuation into this Fault System (Nievoll, 1985).
Es ist eine EW-streichende Störung nördlich des Trofaiach-Becken mit sinistral seitenverschiebender Kinematik. Eine Zugehörigkeit bzw. ein Übergang ins Mur-Mürz-Störungssystem wird diskutiert. (Nievoll, 1985)
Trofaiach-Störung
NCA NE-SW Fault Set
This fault set of NE-SW trending faults within the Northern Calcareous Alps (NCA) includes Annaberg Fault, Isar Fault, Leutasch Fault, Loisach Fault, Pernitz Fault, Pyhrn Fault, Saalach Fault, Salzsteig Fault, and Torscharten Fault amongst other similar orientated faults with same shear sense. These faults were generated during Middle Miocene times as left-lateral strike-slip faults. During Pannonian E-W compression, these NE-SW striking faults were reactivated as right-lateral strike-slip faults. (Peresson & Decker, 1997a, b)
Dieses Störungsset von NE-SW-streichenden Störungen in den Nördlichen Kalkalpen (NKA) beinhaltet die Annaberg-, Isar-, Leutasch-, Loisach-, Pernitz-, Pyhrn-, Saalach-, Salzsteig-, Torscharten- und weitere ähnlich orientierte Störungen mit ähnlicher Kinematik. Diese Störungen entwickelten sich während des mittleren Miozäns als sinistrale Seitenverschiebungen und wurde während des Pannonium als dextrale Seitenverschiebungen reaktiviert. (Peresson & Decker, 1997a, b)
NKA-Störungsset (NE-SW)
For the NW-SE trending brittle fault running from 5 km north of Mariazell to Lilienfeld left-lateral strike-slip diplacement was decribed for Oligocene-Miocene times due to 2 km offset of the Hochwart Fault. Late Miocene right-lateral movement during E-W-compression is expected. (Linzer et al., 2002)
Für die NW-SE-streichende spröde Störung von 5 km nördlich von Mariazell bis Lilienfeld ist eine sinistral-seitenverschiebende Kinematik im Oligozän-Miozän, wegen eines Versatzes der Hochwart Störung von 2 km, bekannt. Spät-Miozäne dextrale Bewegung während E-W-Kompression wird angenommen. (Linzer et al., 2002)
Annaberg Fault
Annaberg-Störung
Salzsteig Fault
This NE-SW trending fault with left-lateral shear sense runs in the area of the Salzsteig. (Decker, 1994; Linzer et al., 2002; Peresson & Decker, 1996)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft entlang des Salzsteiges. (Decker, 1994; Linzer et al., 2002; Peresson & Decker, 1996)
Salzsteig-Störung
Isar Fault
This NE-SW trending fault with left-lateral shear sense runs parallel to the Isar valley. (Eisbacher & Brandtner, 1995, 1996)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft parallel zum Isartales. (Eisbacher & Brandtner, 1995, 1996)
Isar-Störung
Pyhrn Fault
This NE-SW trending fault with left-lateral shear sense runs parallel to the Pyhrnbach Valley. (Decker, 1994; Linzer et al., 2002; Peresson & Decker, 1996)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft parallel zum Verlauf des Pyhrnbaches. (Decker, 1994; Linzer et al., 2002; Peresson & Decker, 1996)
Pyhrn-Störung
Loisach Fault
This NE-SW trending fault with left-lateral movement runs parallel to the Loisach valley. (Eisbacher & Brandtner, 1995, 1996; Linzer et al., 2002)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft parallel zum Loisachtal. (Eisbacher & Brandtner, 1995, 1996; Linzer et al., 2002)
Loisach-Störung
Leutasch Fault
This NE-SW trending fault with left-lateral shear sense is located in the area of the village of Leutasch. (Mählmann & Morlok, 1992)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik befindet sich bei Leutasch. (Mählmann & Morlok, 1992)
Leutasch-Störung
Saalach Fault
This NE-SW trending fault has assumedly left-lateral shear sense and runs parallel to the Saalach Valley. (Tollmann, 1986)
Diese NE-SW-streichende Störung verläuft parallel zum Verlauf des Saalachtales. Es wird ein sinistral seitenverschiebender Kinematik angenommen. (Tollmann, 1986)
Saalach-Störung
Pernitz Fault
This NE-SW trending fault with left-lateral shear sense runs close to the village of Pernitz. (Decker, 1996; Linzer et al., 2002)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft in der Nähe von Pernitz. (Decker, 1996; Linzer et al., 2002)
Pernitz-Störung
Torscharten Fault
This NE-SW trending fault with left-lateral shear sense runs in the area of the Hohe Torscharte. (Frisch & Gawlick, 2003)
Diese NE-SW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft im Bereich der Hohen Torscharte. (Frisch & Gawlick, 2003)
Torscharten-Störung
NE Molasse Fault Set
Nordöstliches Molasse Störungsset
This fault set consists of faults within in the Molasse Basin between Melk in the southwest and Laa/Thaya in the northeast. It is bound by the outcropping crystalline rock suites of the Bohemian Massif to the northwest, and the Alpine Thrust front to the south and southeast. All faults within the basin are blind faults, active until Badenian of mid-Miocene at the latest, solely evidenced by seismic surveys and drillings. (Kröll et al., 2001; Wagner, 1998)
Dieses Störungset besteht aus Störungen des Mollassebeckens zwischen Melk im Südwesten and Laa a.d. Thaya im Nordosten. Es wird im Nordosten von Kristallingesteinen der Böhmischen Masse begrenzt und von der Alpinen Überschiebungsfront im Süden und Südosten. Alle Brüche innerhalb des Beckens sind blinde Störungen, die längstens bis ins Baden des Mittleren Miozäns aktiv waren, und die nur mittels Seismik und Bohrungen nachgewiesen wurden. (Kröll et al., 2001; Wagner, 1998)
This SE dipping and NE-SW striking normal fault delimitates the Moosbierbaum-Horst towards SE. It runs from the west of Langenrohr via Göllersdorf to the castle Schloss Glaswein. To the south, the fault is cut off from the Tullnerfeld Fault. The main deformation event took place during the Karpatian. (Wessely, 2006)
Diese nach SE einfallende, NE-SW streichende Abschiebung begrenzt den Moosbierbaum-Horst nach NE hin. Sie verläuft von westlich von Langenrohr über Göllersdorf bis Schloss Glaswein. Im Süden wird die Störung von der Tullnerfeld-Störung abgeschnitten. Die Hauptbewegungsphase war im Karpatium. (Wessely, 2006)
Stetteldorf Fault
Stetteldorf-Störung
Inventory and concepts of major tectonic boundaries (faults) and overarching fault domains (areally distinct regions with similar fault pattern and properties) in European principal carbonate geothermal reservoirs as identified on mapping and modelling HotLime’s case study areas.
Tectonic Boundary Objects in carbonate geothermal reservoirs of Europe
This NW dipping and NE-SW striking normal fault delimitates the Moosbierbaum-Horst towards NW. It runs from west of Absdorf via Zwentendorf to Moosbierbaum, where it terminates at the Tullnerfeld Fault. The main deformation event took place during the Karpatian. Wessely (2006) describes this fault as Moosbierbaumer-Störung.
Die nach NW einfallende, NE-SW streichende Abschiebung, begrenzt den Moosbierbaum-Horst nach NW hin. Sie verläuft von westlich von Absdorf über Zwentendorf nach Moosbierbaum, wo sie von der Tullnerfeld-Störung abgeschnitten wird. Die Hauptbewegungsphase war im Karpatium. Wessely (2006) beschreibt die Störung als Moosbierbaumer-Störung.
Zwentendorf Fault
Zwentendorf-Störung
Tullnerfeld Fault
This S-dippping, EW-trending normal fault runs from Tulln through the Tullnerfeld south of the river Danube to Oberbierbaum. Wessely (2006) describes this fault as a Moosbierbaumer Südbruch. (Wessely, 2006).
Diese nach S einfallende, grob E-W streichende Abschiebung schneidet den Moosbierbaum-Horst und die ihn nach NW (Zwentendorf-Störung) bzw. SE (Stetteldorf-Störung) begrenzenden Störungen ab. Sie verläuft von Tulln durch das Tullnerfeld südlich der Donau bis Oberbierbaum. Bei Wessely (2006) wird diese Störung als Moosbierbaumer Südbruch beschrieben. (Wessely, 2006)
Tullnerfeld-Störung
Mailberg Fault
This NE-SW striking and SE-dipping fault runs in Austria from Hollabrunn over Mailberg to Laa an der Thaya. North of Laa an der Thaya, the fault runs parallel to the CZ-Austrian border and along the River Thaya. The downward movement of the hanging wall is 700 m at its maximum. (Buchroithner, 1984; Janouschek, 1980; Wessely, 2006)
Die NE-SW streichende, nach SE einfallende Störung verläuft in Österreich von Hollabrunn über Mailberg nach Laa an der Thaya. Nördlich von Laa a. d. Thaya verläuft die Störung parallel zum Grenzverlauf bzw. zum Flussverlauf der Thaya. Das Hangende ist um max. 700 m abgeschoben worden. (Buchroithner, 1984; Janouschek, 1980; Wessely, 2006)
Mailberg-Störung
This NE-SW striking normal fault in Lower Austria runs from Stockerau via Niederhollabrunn to Naglern. The fault is located in the subsurface at about 3000 m below groundlevel, steeply dipping towards SE. There is no topographical expression of this fault at the surface (Rötzel et al., 2009)
Diese NE-SW-streichende Abschiebung in Niederösterreich verläuft von Stockerau via Niederhollabrunn bis Naglern. Die steil nach SE einfallende Störung befindet sich ca. 3000 m unter der Erdoberfläche und zeigt keine geomorphologische Kante an der Oberfläche (Rötzel et al., 2009)
Niederhollabrunn-Störung
Niederhollabrunn Fault
Niederhollabrunn Störung
The fault set comprises mostly N-S striking faults within the Styrian Basin that have no surface expression. They are observed at depth via industrial seismic and borehole data.
Das Störungsset beinhaltet hauptsächlich N-S-streichende Störungen innerhalb des Steirischen Beckens, die keine oberflächliche Morphologie ausbilden. Diese Störungen wurden anhand von Industrieseismik- und Bohrlochdaten im tieferen Untergrund nachgewiesen.
Steirisches Becken Störungsset
Styrian Fault Set
The NNW-SSE striking light-lateral strike-slip fault runs from east of Frohnleiten via Graz to Spielfeld (Tollmann, 1977; Untersweg, 1982, Flügel, 1988, Kröll et al., 1988).
Die NNW-SSE-streichende dextrale Seitenverschiebung mit teiweiser top nach Osten abschiebender Kinematik verläuft östlich von Frohnleiten über Graz nach Spielfeld und ist deutlich im Bereich zwischen Semriach und Stattegger Graben ausgeprägt (Tollmann, 1977; Untersweg, 1982; Flügel, 1988; Kröll et al., 1988).
Leber Fault
Leber-Störung
The E-W striking fault runs from Garrach-Dorf via Weiz to Stubenberg and is part of the Styrian Basin. (Flügel, 1988)
Die E-W-streichende Störung verläuft von Garrach-Dorf über Weiz bis Stubenberg. (Flügel, 1988)
Weiz Fault
Weiz-Störung
Illertal-Störung
Iller-Störung
Iller Fault
N-S trending sinistral strike-slip fault with an oblique normal fault component subparallel to the Iller river valley. Displaces the Alpine Basal Thrust [DE-BY_753] and the Northern Boundary of Subalpine Molasse [DE-BY_789] (Lagally et al. 2009, p 22).
Diese N-S verlaufende sinistrale Blattverschiebung mit abschiebender Komponente verläuft von Immenstadt (Bayern, D) subparallel zum N-S orientierten Streichen des Illertales bis zur deutsch-österreichischen Grenze. Dabei versetzt sie den Nordrand der Faltenmolasse [DE-BY_789]. (Pfiffner, 2011, Zerlauth, 2014)
Iller Valley Fault
Iller Störung
Südwestliche Begrenzung des variszischen Grundgebirges der Böhmischen Masse zum Niederbayerischen Molassebecken. Großräumig NW-SE streichendes, ca. 70° nach SW einfallendes bis saigeres polyphases Störungssystem subparallel zum Verlauf der Donau zwischen Regensburg und Deggendorf, von wo es sich in Teilästen bis nach Österreich hinzieht. Die duktile Hauptbewegungsphase mit vorwiegend dextraler Bewegungsrichtung im Spätvariszikum und dessen miozäne Reaktivierung bildeten ein komplexes Störungssystem mit ausgedehnten Tektonit-Zonen, Bruchstufen und Staffelbrüchen mit Versätzen von bis zu über 1 km. durch ± senkrecht dazu streichende Bayerwald Meridional Störungen [DE-BY_1350] und deren die Stallwanger Furche begrenzende Pendants.
Southwestern boundary of the exposed Variscan basement rock suites of the Bohemian Massif towards Lower Bavaria Molasse Basin. Overall NW-SE trending, approx. 70° SW to vertically dipping polyphase large-scale fault system running subparallel to the Danube river from Regensburg to Deggendorf, continuing in various branches further to Austrian territory. The Late Variscan ductile main displacement phase, a principally dextral movement, and the Miocene brittle reactivation resulted in a complex fault system of extensive tectonite zones, fault scarps and step faults with an overall throw up to more than 1 km.
Donau-Störungssystem
Danube Fault System
Im Donaustörungssystem mit einem Vertikalversatz von bis zu mehr als 1 km, treffen die tiefen, überdeckten Störungen des niederbayerisch-oberösterreichischen Molassebeckens und die gering überdeckten, selten exponierten Störungen der Böhmischen Masse aufeinander. Die Beschreibungen der tiefliegenden Störungen im Molassebecken beziehen sich auf die im 3D-Modell ermittelten Schnittspuren an der Weißjura-Oberfläche bzw. deren Randfazies-Äquivalenten, abgeleitet aus seismischen und Schwere-Messungen sowie vereinzelten Bohrungsbelegen; subseismische Merkmale konnten dabei naturgemäß nicht berücksichtigt werden. Die Beschreibungen der abgeleiteten (gering überdeckten) und kartierten (aufgeschlossenen) Störungen im Kristallin der Böhmischen Masse entsprechen dem im Maßstab von etwa 1:100.000 generalisierten Störungsverlauf an der Geländeoberfläche, wobei flächige Störungszonen aus Tektoniten in den HotLime-Darstellungen als Mittellinie zusammengefasst sind.
The Danube Fault System, featuring a throw of up to more than 1 km, represents the borderline where the blind faults of the Lower Bavaria - Upper Austria Molasse Basin and exposed resp. subcropping faults of the Bohemian Massif converge. The basinal faults, as 3D modelled based on evidence in seismic and gravity surveys and scarce deep drillings, are described as traced on the top of Upper Jurassic strata or its marginal facies equivalents. Conditioned by methodology, subseismic features are neglected. The inferred subcropping and mapped rarely outcropping tectonic boundaries of the Bohemian Massif crystalline rock suites are described generalized equivalent to an approximately 1:100,000 scale, in HotLime spatial representations consolidated to the centerlines of wide fault zones made up of mylonites and cataclastites.
Donaustörungssystem
This NW-SE trending shear zone is the older and ductile part of the Donau fault system with predominantly right-lateral strike-slip movement. (Daurer, 1975; Platzer, 1992; Büttner, 2007; Scheck-Wenderoth et al., 2008).
Diese NW-SE-streichende Scherzone beinhaltet den duktilen Teil des Donau-Störungssystems mit hauptsächlich dextral-seitenverschiebender Bewegungsrichtung. (Daurer, 1975; Platzer, 1992; Büttner, 2007; Scheck-Wenderoth et al., 2008)
Danube Shear Zone
Donau-Scherzone
Ratzing-Kachlet Fault
Ratzing-Kachlet Störung
Inferred southeastern continuation of Paleo-Donaurand Fault Scarp [DE-BY_1237] following the Danube river valley gash.
Dem Donautal-Einschnitt folgende, vermutete südöstliche Fortsetzung des Paläo-Donaurandbruchs [DE-BY_1237].
This NW-SE trending fault is the mostly brittle part of the Donau fault system with predominantly right-lateral strike-slip movement. (Daurer, 1975; Platzer, 1992; Büttner, 2007; Scheck-Wenderoth et al., 2008).
Diese NW-SE-streichende Störung beinhaltet den spröden Teil des Donau-Störungssystems mit hauptsächlich dextral-seitenverschiebender Bewegungsrichtung. (Daurer, 1975; Platzer, 1992; Büttner, 2007; Scheck-Wenderoth et al., 2008)
Danube Fault
Donau-Störung
Haselbach-Patriching Fault
Haselbach-Patriching Störung
Slightly NE-ward arcuate NNW-SSE trending, vertical to subvertical fault truncating the mylonite zones of Aicha-Halser Nebenpfahl [DE-BY_762] in the east.
Leicht NE-wärts gebogen NNW-SSE verlaufende, saigere to subvertikale Störung, die die Mylonitzonen des Aicha-Halser Nebenpfahls [DE-BY_762]im Osten begrenzen.
Paleo-Donaurand Fault Scarp
Paläo-Donaurandbruch
Running from Winzer to Gerading, southwestern intra-basement branch of Donau Fault System southwest of Deggendorf. NW-SE trending ± vertical, moderate throw polyphase fault featuring vein quartz, mylonites and cataclastites. Cutting across a downthrow block of Jurassic carbonates in its northwestern part close to Danube river.
Von Winzer bis Gerading ziehender Südwest-Ast des Donaustörungssystems im Grundgebirge der Böhmischen Masse. NW-SE verlaufende, steilstehende mehrphasige Störung aus Gangquarz, Myloniten und Kataklastiten. Querstörungen im nordwestlichen, Donau-nahen Abschnitt begrenzen eine abgesenkte Scholle jurassischer Karbonate.
NW-SE to WNW-ESE trending continuation of the Aicha-Halser Nebenpfahl along the Danube river valley downriver of Passau featuring brittle faulting segments as well as mylonite zones. Evolved from two phases of mainly dextral movement direction, a Late Varican ductile main phase and a Miocene brittle reactivation (Brandmayr et al. 1997).
Donauleiten Fault
Donauleiten Störung
NW-SE bis WNW-ESE verlaufende Fortsetzung des Aicha-Halser-Nebenpfahles entlang des Donautals unterhalb von Passau mit bruchtektonischen Segmenten sowie Mylonitzonen. Entstanden in zwei Phasen mit vorwiegend dextraler Bewegungsrichtung, einer spätvariszischen duktilen Hauptbewegungsphase und einer miozänen spröden Reaktivierung (Brandmayr et al. 1997).
Donauleiten Subsidiary Faults
Donauleiten Nebenstörungen
WNW-ESE trending vertical to subvertical strike slip faults parallel to and kinematically related with Donauleiten Fault.
WNW-ESE verlaufende, saigere bis subvertikale Blattverschiebungen parallel zu und kinematisch verbunden mit der Donauleiten Störung.
Aicha-Halser Nebenpfahl
Halser Pfahl
Running from Winzer southwest of Deggendorf to Passau northeastern intra-basement branch of Donau Fault System. Predominantly NW-SE trending vertical to steeply SW dipping, moderate throw polyphase fault mainly manifested in extensive zones of mylonites and cataclastites and quartz veins.
Von Winzer bis Passau ziehender Nordost-Ast des Donaustörungssystems im Grundgebirge der Böhmischen Masse. NW-SE verlaufende, steilstehende bis steil SW fallende, polyphase Störung, die in Form ausgedehnter Mylonit- und Kataklastit-Zonen sowie als Gangquarz in Erscheinung tritt.
Main scarp of the Danube Fault System. W-E to NW-SE trending, approx. 70° S to SW dipping fault scarp, in parts step fault, with polyphase kinematics (Late Varican ductile main phase, manifested in tectonite zones of various scale, and Miocene brittle reactivation) establishing the distinctive NE border of the Molasse Basin towards the crystalline rock suites of the Bohemian Massif in an up to more than 1 km throw. Rarely disclosed as mostly covered by Tertiary and Quaternary sediments. In sections, the Danube Fault Scarp is intensely compartmentalised by ± perpendicularly striking Bayerwald Meridional Faults [DE-BY_1350] and the resembling boundary faults of Stallwang Trench (Stallwanger Furche) resulting from late to post-Variscan brittle deformation, reactivated during Late Cretaceous and Paleogene.
Donaurand Fault Scarp
Großer Donau Abbruch
Bayerwald Abbruch
Donaurandbruch
Hauptabbruch des Donaustörungssystems. W-E bis NW-SE verlaufende, ca. 70° nach S bis SW einfallende Bruchstufe, bzw. Staffelbruch, geprägt durch eine mehrphasige Kinematik (spätvariszische duktile Hauptbewegungsphase, unter Bildung von Tektoniten unterschiedlicher Erstreckung, und miozäne spröde Reaktivierung). Mit Sprunghöhen bis zu über 1 km bildet der Donaurandbruch die markante NE Begrenzung des Molassebeckens zu den Kristallingesteinen der Böhmischen Masse. Meist von tertiären und quartären Sedimenten überdeckt, nur in wenigen kurzen Abschnitten aufgeschlossen. Der Donaurandbruch wird durch ± senkrecht dazu streichende Bayerwald Meridional Störungen [DE-BY_1350] und deren die Stallwanger Furche begrenzende Pendants bereichsweise stark zergliedert. Diese Querstörungen sind das Ergebnis einer spät- bis postvariszischen bruchhaft-spröden Deformation und deren Reaktivierung während der Unterkreide und im Alttertiär.
Hengersberger Bucht Faults
Hengersberger Bucht Störungen
Blind faults of the Varican basement burried under Tertiary unconsolidated deposits of Hengersberger Bucht (embayment), inferred from on strike elongation of subcropping faults and basin margins. Roughly paralleling the Donaurand Fault Scarp [DE-BY_698] resp. the northern tail of Deggendorf-Ried Faultsystem [DE-BY_929] and offset by ± W-E trending lateral faults.
Überdeckte Störungen des variszischen Grundgebirges unter den tertiären Lockergesteins- Ablagerungen der Hengersberger Bucht, abgeleitet aus der Verlängerung "aufgeschlossener" Störungen und vermuteter Störungen an den Beckenrändern. In etwa parallel zum Donaurandbruch [DE-BY_698] bzw. dem Nordende des Deggendorf-Ried Störungssystems [DE-BY_929] und von ± W-E verlaufenden Querstörungen versetzt.
Natternberg Faults
Natternberg Störungen
Pair of parallel NW-SE trending inversely arranged subvertical subsidiary faults of Donaurand Fault Scarp, truncated by ± perpendicularly striking Bayerwald Meridional Faults [DE-BY_1350], exposing tectonites of the pediment in an uplifted rhomb horst or push-up, aka positive flower structure. Such structures in between upward convex splay faults imply a reverse vertical component of the strike-slip movement.
Paar NW-SE verlaufender, durch ± senkrecht dazu streichende Bayerwald Meridional Störungen [DE-BY_1350] begrenzter, gegensinnig subvertikaler Nebenstörungen des Donaurandbruchs, zwischen denen die Tektonite der Gebirgsfußfläche in einem aufgepressten rhombenförmigen Horst („positive Blumenstruktur“) zu Tage treten. Solche Strukturen zwischen nach oben konvexen Nebenbrüchen implizieren eine aufschiebende Komponente der Blattverschiebung.
Münster Fault
Münster Störung
WNW-ESE striking, vertical to steeply SSW dipping normal fault of a Donaurand Scarp [DE-BY_698] step fault segment. Northern boundary of a hanging wall block exposing Mesozoic deposits. In the east offset truncated by Ascha-Furth Fault [DE-BY_1537].
WNW-ESE streichende, vertikal bis steil nach SSW einfallende Abschiebung eines Staffelbruch-Segments des Donaurandbruchs [DE-BY_698]. Nördliche Begrenzung einer abgesenkten Scholle mit mesozoischen Ablagerungen. Im Osten von der Ascha-Furth Störung [DE-BY_1537] abgeschnitten.
WNW-ESE striking, vertical to steeply NNE dipping blind normal fault featuring a throw of about 100 m, southward parallel to the Donaurand Fault Scarp [DE-BY_698] and northward subparallel to Straubing Fault [DE-BY_924], in the west truncated by a Bayerwald Meridional Fault [DE-BY_1350], in the east by Ascha-Furth Fault [DE-BY_1537]. Southern boundary of Münster Graben, formed by the hanging wall in between Münster Graben Fault and Donaurand Fault Scarp, and northern boundary of Parkstetten Step, the footwall of Münster Graben Fault and hanging wall of Straubing Fault [DE-BY_1535].
WNW-ESE streichende, vertikal bis steil nach NNE einfallende überdeckte Abschiebung mit einer Sprunghöhe von ca. 100 m, südlich parallel zum Donaurandbruch [DE-BY_698] und nördlich subparallel zur Straubing Störung [DE-BY_924], im Westen von einer Bayerwald Meridional Störung [DE-BY_1350], im Osten von der Ascha-Furth Störung [DE-BY_1537] abgeschnitten. Südgrenze des Münster Grabens, der von der Liegendscholle zwischen Münster Störung und Donaurandbruch gebildet wird, und Nordgrenze der Parkstetten Stufe, der Hangendscholle der Münster Graben Störung und Liegendscholle der Straubing Störung [DE-BY_1535].
Münster Graben Fault
Münster Graben Störung
Steinach-Deggendorf Fault
Steinach-Deggendorf Störung
Northward parallel to the main scarp, WNW-ESE trending, steeply SSW dipping subsidiary fault of Donaurand Fault Scarp [DE-BY_698] as the northern boundary of tectonite occurrances.Multiple dextral displacements by Bayerwald Meridional Faults [DE-BY_1350], Ascha-Furth Fault [DE-BY_1537] and Mitterfels-Bogen Fault [DE-BY_1486].
Nördlich parallel zum Hauptabbruch, WNW-ESE verlaufende, steil nach SSW einfallende Nebenstörung des Donaurandbruchs [DE-BY_698] als nördliche Grenze vom Tektonit Vorkommen. Mehrfach von Bayerwald Meridional Störungen [DE-BY_1350] und den Ascha-Furth [DE-BY_1537] und Mitterfels-Bogen [DE-BY_1486] Störungen dextral versetzt.
Keilberg-Burgberg Faults
Keilberg-Burgberg Störungen
W-E trending subsidiary faults of Donaurand Fault Scarp confining blocks of brecciated Rotliegend deposits in a graben-like structure or on top of an intermediate hanging wall block of a step fault segment of Donaurand Fault Scarp, truncated by Keilberg Fault [DE-BY_761] in the west and Kittenrain Faults [DE-BY_1482] in the east.
W-E verlaufende Nebenstörungen des Donaurandbruchs als Begrenzungen von Schollen brekziierter Rotliegend-Ablagerungen, in Form grabenartiger Vertiefungen oder auf höheren Treppenstufen eines Staffelbruch-Abschnitts des Donaurandbruchs; im Westen von der Keilberg Störung [DE-BY_761], im Osten von den Kittenrain Störungen [DE-BY_1482] begrenzt.
NW-SE striking, approx. 70° NE dipping train of blind normal faults. Antithetic, probably conjugate fault system to the Donaurand Fault Scarp [DE-BY_698]. Part of northeastern fringe of Regensburg-Straubing Trough.
NW-SE streichender Störungszug ca. 70° nach NE einfallender Abschiebungen. Antithetisches, wahrscheinlich konjugiertes Störungssystem zum Donaurandbruch [DE-BY_698]. Teil des Nordost-Rands der Regensburg Straubinger Senke.
Niederachdorf-Platting Fault
Sünching-Plattling Störung
Niederachdorf-Plattling Störung
Plattling Fault
Plattling Störung
NW-SE striking, approx. 70° NE dipping blind antithetic normal fault.
NW-SE streichende, ca. 70° nach NE einfallende antithetische Abschiebung.
NW-SE striking, approx. 70° NE dipping blind antithetic normal fault with a throw of about 80 m. In its southeastern segment southwestern boundary of Parkstetten Step, the hanging wall of Münster Graben Fault [LfU-BY_1539] and footwall of Straubing Fault.
NW-SE streichende, ca. 70° nach NE einfallende antithetische Abschiebung mit einem Verwurf von ca. 80 m. In ihrem südöstlichen Abschnitt Südwestgrenze der Parkstetten Stufe, der Hangendscholle der Münster Graben Störung [LfU-BY_1539] und Liegendscholle der Straubing Störung.
Straubing Fault
Straubing Störung
Kalkberg Fault
Kalkberger Aufschiebung
Kalkberger Bruch
Kalkberg Störung
NW-SE trending, approx. 80° SW dipping reverse fault running from Vilshofen to Neuburger Wald. Regime and kinematics is proved by observation / measuremet in few outcrops. Northeastern limit of Ortenburg Depression featuring a throw of up to 400 m.
NW-SE verlaufende, ca. 80° nach SW einfallende Störung mit aufschiebendem Bewegungssinn zwischen Vilshofen und Neuburger Wald. Verlauf und Kinematik ist durch Beobachtungen in einigen Aufschüssen gesichert. Nordöstliche Begrenzung des Ortenburger Senkungsfelds mit einer Sprunghöhe bis zu 400 m.
Wolfach Fault
Wolfach Störung
NNW-SSE striking, approx. 80° NNE dipping normal fault running from Vilshofen to Dorfbach. Western limit of Ortenburg Depression featuring a throw up to 170 m.
NNW-SSE streichende, ca. 80° nach NNE einfallende Abschiebung zwischen Vilshofen und Dorfbach. Westliche Begrenzung des Ortenburger Senkungsfelds mit einer Sprunghöhe bis zu 170 m.
The 110 km long sub fault system branches off from the Salzach fault north of the Tauern window near Zell and strikes with 70° in the south and 30° in the north (Decker et al., 1994). The main deformation of sinistral transpressive character leads to a vertical displacement of 700-2000 m. It offsets the southern margin of the Northern Calcareous Alps by 10-15 km (Linzer et al., 2002).
Das 110 km lange Teilstörungssystem, das nördlich des Tauernfensters bei Zell aus der Salzach-Störung abzweigt, streicht mit 70° im Süden bzw. 30° im Norden (Decker et al., 1994). Die Hauptbewegungsphase hat sinistral transpressiven Charakter und führt zu 700-2000 m vertikalem Versatz. Sie versetzt den Kalkalpensüdrand um 10-15 km (Linzer et al., 2002).
Königsee-Lammertal-Traunsee Subfault System
Königsee-Lammertal-Traunsee-Teilstörungssystem
Rust Fault System
This fault system consists of several N-S striking faults towards E and W, which runs from Schützen am Gebirge over St. Margarethen and Rust to the Austro-Hungarian border and supposable to Sopron. These presumably post-Miocene faults limit the so-called Ruster Höhenzug and were possibly originally developed as lateral dislocation. (Kröll et al., 1993; Häusler et al., 2010)
Dieses Störungssystem besteht aus mehreren N-S streichenden, nach E und W einfallenden Abschiebungen, die sich von Schützen am Gebirge über St. Margarethen und Rust bis zur österreichisch-ungarischen Grenze und vermutlich bis Sopron hinziehen. Diese vermutlich postmiozänen Abschiebungen begrenzen den sogenannten Ruster Höhenzug und wurden möglicherweise ursprünglich als Seitenverschiebungen angelegt. (Kröll et al., 1993; Häusler et al., 2010)
Rust-Störungssystem
Telfs Subfault System
This ca. 35 km long, approximately WNW-ESE trending Subfault System extends from Fernpass to Imst and Zirl, including the Telfs shear zone and Telfs fault. A Cretaceous system is described with an offset between 10-20 km which were caused during the displacement of the Inntal nappe and the dextral lateral kinematics during Miocene. (Eisbacher, 1995, 1996)
Dieses WNW-ESE-streichende, ca. 35 km lange Teilstörungssystem verläuft vom Fernpass über Imst bis Zirl und beinhaltet die Telfs-Scherzone und Telfs-Störung. Es wird eine kreidezeitliche Anlage beschrieben mit Versatzweiten zwischen 10-20 km die während der Überschiebung der Inntal-Decke und durch Miozäne dextral seitenverschiebende Kinematik zustande gekommen sind. (Eisbacher, 1995, 1996)
Telfs-Teilstörungssystem
The WNW-ESE striking dextral strike-slip fault runs from the Fern Pass south of Biberwier via Telfs to Kematen/Tirol (Eisbacher and Brandner, 1995, 1996).
Die WNW-ESE-streichende dextrale Seitenverschiebung verläuft vom Fernpass südlich von Biberwier über Telfs nach Kematen in Tirol (Eisbacher and Brandner, 1995, 1996).
Telfs-Störung
Telfs Fault
Vitis-Pribyslav Fault System
This NNE-SSW striking, steeply WNW dipping fault system runs from Perg via Zwettl and Vitis to Slavonice (CZ), where it continues in the Czech Republic. The ductile main movement phase, similar to the Rodl fault system, is applied to the Late Variscan, with mainly sinistral direction of motion. It is assumed, that a brittle Miocene reactivation holds the same motion kinematic. (Brandmayr, 1997, Büttner, 2007, Lehnhard, 2007)
Dieses NNE-SSW streichende, steil nach WNW einfallende Störungssystem zieht sich von Perg über Zwettl und Vitis bis Slavonice (CZ), wo es sich in der Tschechischen Republik weiter fortsetzt. Die duktile Hauptbewegungsphase wird, analog zum Rodl-Störungssystem, auf das Spätvariszikum gelegt, mit hauptsächlich sinistraler Bewegungsrichtung. Von einer spröden miozänen Reaktivierung mit selber Bewegungskinematik wird ebenfalls ausgegangen. (Brandmayr, 1997, Büttner, 2007, Lehnhard, 2007)
Vitis-Pribyslav-Störungssystem
Wiesmath-Störung
Wiesmath Fault
The approximately E-W striking fault runs from Stickelberg to Schwarzenbach.
Die in etwa E-W-streichende Störung verläuft von Stickelberg bis Schwarzenbach.
Dieses Störungsset besteht aus ENE-WSW-streichenden Störungen in den Nördlichen Kalkalpen (NKA). Diese Störungen entwickelten sich wahrscheinlich im mittleren Miozän als sinistrale Seitenverschiebungen und wurden während E-W-Kompression im Pannon als dextrale Seitenverschiebungen reaktiviert. (Peresson & Decker, 1997a, b).
The fault set contains ENE-WSW trending faults within the Northern Calcareous Alps (NCA). These faults were probably generated during Middle Miocene times as left-lateral strike-slip faults. During Pannonian E-W compression, they might have been reactivated as right-lateral strike-slip faults (Peresson and Decker, 1997a, b).
NCA ENE-WSW Fault Set
NKA-Störungsset (ENE-WSW)
The E-W trending brittle thrust fault of in the Northern Calcareous Alps runs from Altenmarkt/St. Gallen to 6 km east Kienberg and is juxtaposed by the left-lateral Göstling fault. (Decker et al., 1994)
Die E-W-streichende spröde Überschiebung in den nördlichen Kalkalpen verläuft von Altenmarkt/St. Gallen bis 6 km östlich von Kienberg und wird von der Göstling-Störung sinistral versetzt. (Decker et al., 1994)
Königsberg Fault
Königsberg-Störung
Toplitz Fault
The ENE-WSW striking fault runs from the east bank of the lake Hallstatt via Bad Aussee across the lakes Grundlsee and Toplitzseee to the west of the Hebenkas-Spitze. (Tollmann, 1986)
Die ENE-WSW streichende Störung verläuft vom Ostufer des Hallstätter Sees über Bad Aussee durch den Grundlsee und Toplitzseee bis westlich der Hebenkas-Spitze. (Tollmann, 1986)
Toplitz-Störung
This fault set consists of NW-SE striking faults within the Northern Calcareous Alps (NCA) including Gosaukamm Fault, Gosausee Fault, Hochwart Fault, Lofer Fault, Scharnitzsattel Fault, Windischgarsten Fault, and Wolfgangsee Fault and other similar orientated faults with same kinematics. These faults were generated in the Late Eocene-Oligocene as right-lateral strike-slip faults. During Pannonian E-W compression, these NW-SE striking faults were reactivated as left-lateral strike-slip faults. (Peresson & Decker, 1997a, b)
Dieses Störungsset besteht aus NW-SE-streichenden Störungen in den nördlichen Kalkalpen (NKA) und beinhaltet die Gosaukamm-, Gosausee, Hochwart-, Lofer, Scharnitzsattel-, Windischgarsten-, Wolfgangsee- und weitere ähnlich orientierte Störungen mit derselben Kinematik. Diese Störungen entstanden im späten Eozän bis Oligozän als dextrale Seitenverschiebungen und wurden während E-W-Kompression im Pannonium als sinistrale Seitenverschiebungen reaktiviert. (Peresson & Decker, 1997a,b)
NCA NW-SE Fault Set
NKA-Störungsset (NW-SE)
Hochwart Fault
This NW-SE trending fault with right-lateral shear sense runs through the area of the mountain Hochwart. (Linzer et al., 1997, 2002; Peresson & Decker, 1997)
Diese NW-SE-streichende Störung mit dextral-seitenverschiebender Kinematik verläuft im Bereich des Hochwart. (Linzer et al., 1997, 2002; Peresson & Decker, 1997)
Hochwart-Störung
This E-W trending fault is located in the area of the lake Spullersee. (Tollmann, 1986)
Diese E-SW-streichende Störung befindet sich im Bereich des Spullersees. (Tollmann, 1986)
Spullersee Fault
Spullersee-Störung
This NW-SE trending fault consists of two fault strands running parallel to each other SW and NE of Mt. Wendelstein (DE) from Fischbachau to Oberaudorf. (Frisch & Gawlick, 2003)
Diese NW-SE-streichende Störung verläuft mit zwei Störungsästen von Fischbachau bis Oberaudorf SW und NE vom Wendelstein (DE). (Frisch & Gawlick, 2003)
Wendelstein Fault
Wendelstein-Störung
Windischgarsten Fault
This NW-SE trending fault with a right-lateral shear sense is located in the area of the town of Windischgarsten. (Decker et al., 1994; Peresson & Decker, 1997; Linzer et al., 2002)
Diese NW-SE-streichen Störung in den nördlichen Kalkalpen befindet sich im Bereich Windischgarsten mit dextral-seitenverschiebender Kinematik. (Decker et al., 1994; Peresson & Decker, 1997; Linzer et al., 2002)
Windischgarsten-Störung
Scharnitzsattel Fault
The NW-SE trending fault with right-lateral shear sense is located in the area of the Scharnitzsattel. (Ortner, 2001)
Diese NW-SE-streichen Störung in den nördlichen Kalkalpen verläuft im Bereich des Scharnitzsattel mit dextral-seitenverschiebender Kinematik. (Ortner, 2001)
Scharnitzsattel-Störung
Lofer Fault
This NW-SE trending fault with right-lateral shear sense is located within the Northern Calcercous Alps close to the town of Lofer. (Frisch & Gawlick, 2003)
Diese NW-SE-streichen Störung verläuft in den nördlichen Kalkalpen bei Lofer mit dextral-seitenverschiebender Kinematik. (Frisch & Gawlick, 2003)
Lofer-Störung
Wolfgangsee Fault
This NW-SE trending fault with right-lateral shear sense is located in the area of the Lake Wolfgang. (Decker et al., 1993, 1994; Peresson & Decker, 1997a, b; Frisch & Gawlick, 2003)
Diese NW-SE-streichen Störung befindet sich in den nördlichen Kalkalpen im Bereich des Wolfgangsees mit dextral-seitenverschiebender Kinematik. (Decker et al., 1993, 1994; Peresson & Decker, 1997a, b; Frisch & Gawlick, 2003)
Wolfgangsee-Störung
Gosaukamm Fault
The NW-SE trending fault with right-lateral shear sense runs through the area of the Gosaukamm. (Frisch & Gawlick, 2003)
Diese NW-SE streichende Störung mit dextral-seitenverschiebender Kinematik verläuft im Bereich des Gosaukammes. (Frisch & Gawlick, 2003)
Gosaukamm-Störung
Gosausee Fault
This NW-SE trending fault with right-lateral shear sense runs in the area of the Gosau lakes. (Frisch & Gawlick, 2003; Wagreich & Decker, 2001)
Diese NW-SE streichende Störung mit dextral-seitenverschiebender Kinematik verläuft im Bereich der Gosauseen. (Frisch & Gawlick, 2003; Wagreich & Decker, 2001)
Gosausee-Störung
Salzach-Ennstal-Mariazell-Puchberg Fault System
A WSW-ENE striking fault system of approximately 400 km in length, running from the western Tauern Window to the Vienna basin and up to 70 km of sinistral offset. The deformation holds a gradient from ductile (W) to brittle ductile (central region) to brittle (E). The Salzach-Ennstal-Mariazell-Puchberg Fault System is composed of W to E from the Salzach fault (brittle northern edge of the Tauern window), the Ennstal fault (southern edge of the northern Kalkalpen) and the Mariazell-Puchberg fault. (Linzer, 2002)
Ein WSW-ENE streichendes Störungssystem von ca. 400 km Länge, das sich vom westlichen Tauernfenster bis zum Wiener Becken hinzieht und bis zu 70 km sinistralen Versatz aufweist. Die Deformation weist einen Gradienten von duktil (W) über spröd-duktil (Zentralbereich) bis spröd (E) auf. Das Salzach-Ennstal-Mariazell-Puchberg-Störungssystem setzt sich von W nach E aus dem Salzach-Störung (spröder Nordrand des Tauernfensters), der Ennstal-Störung (südlicher Rand der nördlichen Kalkalpen) und der Mariazell-Puchberg-Störung zusammen. (Linzer, 2002)
Salzach-Ennstal-Mariazell-Puchberg-Störungssystem
Ennstal-Teilstörungssystem
The WSW-ENE trending fault system is part of the Salzach-Ennstal-Mariazell-Puchberg Faultsystem. Left-lateral movement is described (Linzer et al., 2002).
Diese WSW-ENE-streichende Störung verläuft parallel zum Salzachtal und ist Teil des Salzach-Ennstal-Mariazell-Puchberg-Störungssystem. Sinistral-seitenverschiebende Kinematik ist beschrieben (Linzer et al., 2002).
Ennstal Subfault System
Mariazell-Puchberg-Teilstörungssystem
Mariazell-Puchberg Subfault System
The WSW-ENE trending fault system runs parallel to the valley of the river Salzach and is part of the Salzach-Ennstal-Mariazell-Puchberg Faultsystem. Left-lateral movement is described (Linzer et al., 2002).
Salzach Subfault System
Salzach-Teilstörungssystem
This WSW-ENE trending fault runs parallel to the valley of the river Salzach and is part of the Salzach-Ennstal-Mariazell-Puchberg Faultsystem. Left -lateral movement is described (Linzer et al., 2002).
Salzach Fault
Salzachtal-Störung
Freyenstein Fault System
Freyenstein-Störungssystem
This ca. 45 km long NE-SW, partly NNE-SSW trending Subfault System extends from Windpassing to Freyenstein, Ysper and Klein-Nondorf (SW of Grafenschlag). It is part of the Vitis-Pribyslav Fault System at the eastern end of the South Bohemian Batholith. It includes an approximately 500 m thick ductile, SE-dipping mylonitic normal shear zone with top S/SE sense of shear dated to the Late Variscian. Late Miocene reactivation, with left-lateral movement, is assumed (Griesmeier et al., 2016).
Dieses ca. 45 km lange, NE-SW-, teilweise NNE-SSW-streichende Teilstörungssystem verläuft von Windpassing nach Freyenstein und nördlich der Donau weiter nach Ysper und Klein-Nondorf (SW Grafenschlag). Es ist Teil des Vitis-Prybislav-Störungssystems am Ostrand des Südböhmischen Batholithen. Es beinhaltet eine ca. 500 m mächtige duktile SE-einfallende mylonitische Scherzone mit top nach S/SE abschiebender Kinematik aktiv während des spät-Variszikums. Eine Miozäne Reaktivierung mit sinistral-seitenverschiebender Bewegung ist beschrieben (Griesmeier et al., 2016).
Niedere Tauern Southern Margin Fault System
This ca. 70 km long, approximately ESE-WNW trending Fault System extends from St. Michael im Lungau, following the basins of Tamsweg and Seetal to Oberwölz and Oberzeiring (east of the Pöls Valley) including parallel trending faults (Reinecker, 2000; Eder & Neubauer, 2000). It was initiated as ductile nappe boundaries during Cretaceous times and as S-dipping normal fault with top NE sense of shear active in the Paleogene. Reactivation with left-lateral strike-slip movement and the formation of pull-apart basins during Miocene times is described (Eder & Neubauer, 2000).
Dieses etwa ESE-WNW streichende ca. 70 km lange Störungssystem zieht von St.Michael im Lungau über das Tamsweg- und Seetal-Becken bis Oberwölz und weiter nach Oberzeiring (östlich des Pölstals) und fasst parallel streichende Störungen in diesem Bereich zusammen (Reinecker, 2000; Eder & Neubauer, 2000). Es wurde als Deckengrenzen der Oberkreide angelegt und war vermutlich im Paläogen als dextral seitenverschiebende und top NE abschiebende Störungen aktiv. Diese wurden als sinistrale Seitenverschiebungen mit der Bildung von pull-apart-Becken im Miozän reaktiviert (Eder & Neubauer, 2000).
Niedere Tauern Südrand Störungssystem
Lower Tauern Southern Margin Fault System
Tamsweg-Becken-Teilstörungssystem
Tamsweg Basin Subfault System
This fault is part of the Niedere Tauern Südrand Fault System and borders respectively divided the Tamsweg basin in a western and eastern part. The strike-slip faults were reactivated contemporaneously with the formation of pull-apart basins during the Miocene (Eder & Neubauer, 2000; Wölfler et al., 2011).
Dieses Teilstörungssystem ist Teil des Niedere Tauern Südrand-Störungssystems und begrenzt bzw. teilt das Tamsweg-Becken in einen östlichen und westlichen Teil. Die Seitenverschiebungen wurden mit der Bildung von pull-apart-Becken im Miozän angelegt (Eder & Neubauer, 2000; Wölfler et al., 2011).
Seetal Fault
Seetal-Störung
The approximately E-W trending fault is part of the Niedere Tauern Südrand Fault System and runs from St. Margarethen/Lungau to Murau. Left-lateral strike-slip faults were reactivated contemporaneously with the formation of pull-apart basins during the Miocene (Eder & Neubauer, 2000).
Die in etwa EW-streichende Störung ist Teil des Niedere Tauern Südrand-Störungssystems und verläuft von St. Margarethen im Lungau bis Murau. Die sinistralen Seitenverschiebungen wurden mit der Bildung von pull-apart-Becken im Miozän reaktiviert (Eder & Neubauer, 2000).
Niedere-Tauern-Störung
Niedere Tauern Fault
The approximately E-W trending fault is part of the Niedere Tauern Südrand Fault System and runs from Weißpriach to Teufenbach. Left-lateral strike-slip faults were reactivated contemporaneously with the formation of pull-apart basins during the Miocene (Eder & Neubauer, 2000).
Die in etwa EW-streichende Störung ist Teil des Niedere Tauern Südrand-Störungssystems und verläuft von Weißpriach bis Teufenbach. Die sinistralen Seitenverschiebungen wurden mit der Bildung von pull-apart-Becken im Miozän reaktiviert (Eder & Neubauer, 2000).
Lower Tauern Fault
Trojeralm Fault Set
This subfault system consists of NW-SE trending parallel mylonitic and brittle strike-slip faults including the Trojeralm-, Fleischbachkees-, and Kalsertal Fault. (Senarclens-Grancy, 1959)
Ist ein Störungsset von NW-SE-streichenden parallelen mylonitischen und spröden Seitenverschiebungen, welche die Trojeralm-, Fleischbachkees- und Kalsertal-Störung beinhaltet. (Senarclens-Grancy, 1959)
Trojeralm-Störungsset
Eine Deckengrenze beschreibt in Österreich einen diskreten, spröden oder duktilen Scherhorizont zwischen tektonischen Einheiten (z.B. Decken, Deckensysteme). „Diskret“ bezieht sich hier auf den Kartenmaßstab, denn im Gelände kann eine Deckengrenze einer diffusen tektonischen Melangezone, mit Elementen beider Einheiten die sie trennt, entsprechen (Hintersberger et al. 2017)
Deckengrenze in Österreich
In Austria, a nappe boundary describes a discrete, brittle or ductile, shearing horizon between tectonic units (e.g. nappes, nappe systems). In this definition, „discrete“ refers to map scale, since in the field a nappe boundary can correspond to a diffuse tectonic mélange zone with elements of both units that it separates (Hintersberger et al. 2017)
Nappe Boundary in Austria
This nappe system is the lowermost Austroalpine element above the Penninic Nappes on the eastern edge of the Alps, which overlies the Penninic nappes in the Rechnitz Window Group. The base of the Semmering-Wechsel Nappe System can be found between St. Michael/Obersteiermark and Gloggnitz, a small segment also crops out at Hohentauern.
Dieses Deckensystem stellt das tiefste ostalpine Element über den Penninischen Decken am Alpenostrand dar, das die Penninischen Decken im Bereich der Rechnitzer Fenstergruppe überlagert. Die Basis des Semmering-Wechsel Deckensystem kann zwischen St. Michael in der Obersteiermark und Gloggnitz beobachtet werden, ein sehr kleiner Abschnitt auch bei Hohentauern.
Basis des Semmering-Wechsel-Deckensystems
Base of the Semmering-Wechsel Nappe System
The base of these nappes lies, for the most part, in Styria in the area between St. Michael/Obersteiermark and Gloggnitz (Lower AustrIa) and crops out as well southwest of Trieben. The Grauwackenzone nappes overlie the Silvretta-Seckau Nappe System and are overlain by the Tirolic-Noric Nappe System. During the Eoalpine event in the Cretaceous (85-135 Ma),they were sheared off from their basement and overthrusted towards northwest (adapted from Froitzheim et al., 2008).
Die Basis dieser Decken liegt großteils in der Steiermark zwischen St.Michael in der Obersteiermark und Gloggnitz (Niederösterreich) und ist auch südwestlich von Trieben aufgeschlossen. Die Decken der Grauwackenzone liegen über dem Silvretta-Seckau-Deckensystem und werden vom Tirolisch-Norischen Deckensystem überlagert. Während des eoalpidischen Ereignisses wurden sie in der Kreide (zwischen 85 und 135 Ma) von ihrem Untergrund abgeschert und gegen Nordwesten überschoben (verändert nach Froitzheim et al., 2008).
Basis des Grauwackenzone-Deckensystems
Base of the Greywacke Zone Nappe System
The Modereck Nappe system overlies the Venediger Nappe System in the Tauern Window, therefore its base separates the Subpenninic units throughout the Tauern Window (Pestal et al., 2009).
Die Basis des Modereck-Deckensystems ist im Tauernfenster zu finden und trennt die Modereck Decken vom ebenfalls subpenninischen Venediger-Deckensystem (Pestal et al., 2009).
Base of the Modereck Nappe System
Basis des Modereck-Deckensystems
The base of the Glockner Nappe system is an important, mainly S-dipping thrust fault in the Tauern window which was mainly active during Cretaceous times. It thrusts the Penninic Glockner Nappe system onto the underlying Subpenninic Venediger and Modereck Nappe systems. It can be observed throughout the Tauern Window between east of the Brenner pass in the west and Gmünd and Katschberg in the east (Staub, 1924).
Die Basis des Glockner-Deckensystems ist eine wichtige, hauptsächlich nach S einfallende Überschiebung im Tauernfenster, die hauptsächlich in der Kreide aktiv war. Diese Deckengrenze kann im gesamten Tauernfenster zwischen dem Brennerpass im Westen und Gmünd und Katschberg im Osten beobachtet werden. Sie überschiebt das penninische Glockner-Deckensystem über die liegenden subpenninischen Venediger- bzw. Modereck-Deckensysteme (Staub, 1924).
Basis des Glockner-Deckensystems
Base of the Glockner Nappe System
This tectonically highest Penninic nappe system in the north and south of the Tauern Window overthrusts the Glockner Nappe System at its base (Schuster et al. 2006).
Dieses tektonisch höchste penninisches Deckensystem im Norden und Süden des Tauernfensters überschiebt an seiner Basis das Glockner-Deckensystem (Schuster et al.. 2006).
Basis des Matrei-Nordrahmen-Zone-Deckensystems
Base of the Matrei Nordrahmen Zone Nappe System
The Radstadt Nappe System is the northern Lower Austroalpine part of the Tauern Window above the Penninicum and has been integrated in the Alpine orogenic wedge during Upper Cretaceous (Pestal et al., 2009).
Das Radstadt-Deckensystem stellt den Unterostalpinen nördlichen Rahmen des Tauernfensters über dem Penninikum dar und wurde in der Oberkreide in den Alpinen Orogenkeil eingebaut (Pestal et al., 2009).
Base of the Radstadt Nappe System
Basis des Radstadt-Deckensystems
The base of this nappe system of the Moldanubian Nappes seperates the Drosendorf nappe system from the Ostrong Nappe System, which it overthrusts. The base of the Drosendorf Nappe System crops out between Ybbs/Donau and Brand and in smaller parts around Goschenreith and Drosendorf.
Die Basis des Drosendorf-Deckensystems des Moldanubikums trennt dieses vom überschobenen Ostrong-Deckensystem. Sie ist zwischen Ybbs and der Donau und Brand aufgeschlossen, sowie in kleinern Teilen um Goschenreith und Drosendorf.
Base of the Drosendorf Nappe System
Basis des Drosendorf-Deckensystems
The Ostrong Nappe System, the lowermost system of the Moldanubian Nappes, is overthrusted by the Drosendorf and Gföhl Nappe Systems. The intrusion of the Southern Bohemian Batholith (300-340 Ma) makes up a great part of the nappe system and caused a high-temperature and low-pressure metamorphism. Its base can only be observed around Nöstling.
Das Ostrong-Deckensystem, das unterste Deckenystem der Moldanubischen Decken, wird von den Drosendorf- und Gföhl-Deckensystemen überlagert. Die Intrusion des Südböhmischen Batholiths (300-340 Ma) hat eine Hochtemperatur-Niederdruck-Metamorphose zur Folge. Die Basis des Ostrong-Deckensystems ist nur bei Nöstlig aufgeschlossen.
Base of the Ostrong Nappe System
Basis des Ostrong-Deckensystems
Apart from a small part west of the Brenner Pass in Tirol, the base of this nappe system can be observed in Carynthia and Styria between Bad Kleinkirchheim and Gasen. The Drauzug-Gurktal-Nappes overthrust the Ötztal-Bundschuh and Koralpe Wölz Nappe Systems in shallow reverse faults (Froitzheim et al., 2008).
Abgesehen von einem kleinen Teil westlich des Brennerpasses ist die Basis dieses Deckensystems in Kärnten und der Steiermark zwischen Bad Kleinkirchheim und Gasen aufgeschlossen. Das Drauzug-Gurktal-Deckensystems überfährt in flachen Überschiebungen das Ötztal-Bundschuh- und das Koralpe-Wölz-Deckensystem (Froitzheim et al., 2008).
Base of the Drauzug-Gurktal Nappe System
Basis des Drauzug-Gurktal-Deckensystems
This nappe system includes the Ötztal Nappe to the west and the Bundschuh Nappe to the east of the Tauern Window. The base of these nappes seperates the Ötztal-Bundschuh Nappe System from the overthrusted Koralpe-Wölz Nappe system (Froitzheim et al., 2008).
Dieses Deckensystem umfasst die Ötztal-Decke westlich und die Bundschuh-Decke östlich des Tauernfensters. Die Basis dieser Decken trennt das Ötztal-Bundschuh-Deckensystem vom überschobenen Koralpe-Wölz-Deckensystem. (Froitzheim et al., 2008).
Basis des Ötztal-Bundschuh-Deckensystems
Base of the Ötztal-Bundschuh Nappe System
The base of the Juvavic Nappe System extends from southwest of Salzburg in ENE direction to west of Wiener Neustadt. The Juvavic Nappes were detached from their basement and thrust onto the future Tirolic-Noric Nappe System as early as the Early Upper Jurassic (about 160 Ma). This probably occurred, in part, during the obduction of units from the Neotethys Ocean (Meliaticum), but also partly during a transpressive regime in the Late Upper Jurassic and Early Lower Cretaceous (adapted from Schmid et al., 2004).
Die Basis des Juvavischen Deckensystem erstreckt sich von südwestlich von Salzburg in Richtung ENE bis westlich von Wiener Neustadt. Die Decken wurden bereits ab dem frühen Oberjura (ca. 160 Ma) von ihrem Untergrund abgelöst und auf das zukünftige Tirolisch-Norische Deckensystem aufgeschoben. Dies geschah wahrscheinlich zum Teil im Zuge der Obduktion von Einheiten aus dem Neotethys-Ozean (Meliatikum), zum Teil aber auch in einem transpressiven Regime im späten Oberjura und in der frühen Unterkreide (verändert nach Schmid et al., 2004).
Base of the Juvavic Nappe System
Basis des Juvavischen Deckensystems
Parts of the base of the Tirolic Noric Nappe System can be traced throughout Austria, from southwest of Vorarlberg in ENE direction to west of Wiener Neustadt. The system contains nappes, sheared off in early Lower Cretaceous times (135 Ma), overthrusting the Bajuvaric Nappe System.
Teile der Basis des Tirolisch-Norischen Deckensystems können quer durch Österreich vom Südwesten Vorarlbergs in Richtung ENE bis westlich von Wiener Neustadt verfolgt werden. Das Tirolisch-Norische Deckensystem besteht aus Decken, die ab der frühen Unterkreide (ca. 135 Ma) abgeschert und über das Bajuvarische Deckensystem geschoben wurden.
Base of the Tirolic Noric Nappe System
Basis des Tirolisch-Norischen Deckensystems
The base of the Bajuvaric Nappe System crops out in Vorarlberg and can be traced from south of Gmunden (Upper Austria) in ENE direction to southwest of Vienna. The system contains nappes, sheared off in the middle Lower Cretaceous (120 Ma) and forms the lowermost nappe system of the Northern Calcareous Alps (Schmid et al, 2004).
Die Basis des Bajuvarischen Deckensystems ist in Vorarlberg aufgeschlossen und kann von südlich von Gmunden (Oberösterreich) nach ENE bis südwestlich von Wien verfolgt werden. Die Decken wurden in der frühen Unterkreide (ca. 120 Ma) abgeschert und bilden das unterste Deckensystem der nördlichen Kalkalpen (Schmid et al, 2004).
Basis des Bajuvarischen Deckensystems
Base of the Bajuvaric Nappe System
The base of the nappe system can be observed between east of the Brenner Pass and southwest of Mattersburg. The exhumation of the units took place in the Upper Cretaceous (from 92 Ma) by thrust faults in the underlying parts and normal faults in the overlying parts of the nappe stack. Therefore, the Koralpe Wölz Nappe System represents a metamorphic extrusion wedge which originated during the Eoalpine event. (Froitzheim et al., 2008).
Die Basis dieses Deckensystem kann zwischen dem Brennerpass (E) und südwestlich von Mattersburg beobachtet werden. Die Exhumation der Einheiten erfolgte in der Oberkreide (ab 92 Ma) durch Überschiebungen im liegenden und Abschiebungen im hangenden Teil des Deckenstapels. Demnach stellt das Koralpe-Wölz-Deckensystem einen metamorphen Extrusionskeil dar, der während des eoalpidischen Ereignisses entstand (Froitzheim et al., 2008).
Base of the Koralpe-Wölz Nappe System
Basis des Koralpe-Wölz-Deckensystems
The base of the Upper Penninic Nappes can in Austria be found in Vorarlberg, the southwest border of Tirol to Switzerland and from north of Ybbsitz in ENE direction to west of Vienna. They were formed during the closure of the Piemont-Ligurian Ocean, which began in the middle Upper Cretaceous and lasted until the Eocene. The greater part of the oceanic crust was subducted during this process, whereby the Upper Penninic nappes were overthrust by the Austroalpine nappes (Froitzheim et al., 2008).
Die Basis der Oberen Penninischen Decken ist in Österreich in Vorarlberg und der südwestlichen Grenze von Tirol zu finden, sowie von Ybbsitz in Richtung ENE bis in den Westen von Wien. Diese Decken entstanden bei der Schließung des Piemont-Ligurischen Ozeans, die in der mittleren Oberkreide einsetzte und bis ins Eozän andauerte. Bei diesem Prozess wurde der größte Teil der ozeanischen Kruste subduziert. Dabei wurden die Oberen Penninischen Decken von den Ostalpinen Decken überschoben (Froitzheim et al., 2008).
Base of the Upper Penninic Nappes
Basis der Oberen Penninischen Decken
The Middle Penninic Nappes and their base can in Austria only be found in the Engadin Window. For the most part, they contain rocks of the Iberia-Briançonnais microcontinent and show no pressure-enhanced metamorphism like the Lower Penninic nappes (Froitzheim et al., 2008).
Die Basis der Mittleren Penninischen Decken ist in Österreich ausschließlich im Unterengadiner Fenster zu finden. Zum größten Teil bestehen sie aus Gesteinen des Ibera-Briançonnais-Mikrokontinent und zeigen keine druckbetonte Metamorphose wie die Unteren Penninischen Decken (Froitzheim et al., 2008).
Base of the Middle Penninic Nappes
Basis der Mittleren Penninischen Decken
The base of the Lechtal Nappe of the Bajuvaric Nappe System overthrusting the Allgäu Nappe can be observed north of the Lech Valley in Vorarlberg northwest of Lech and in Tirol between Hinterhornbach and Musau. It manifests strikingly in mainly shallow S- to SW-dipping thrusts.
Die Basis der Lechtal Decke des Bajuvarischen Deckensystems überschiebt die Allgäu Decke und kann nördlich des Lechtales in Vorarlberg nordwestlich von Lech und in Tirol zwischen Hinterhornbach und Musau beobachtet werden. Die Überschiebung ist unterhalb der Höllhörner, an der Jochspitze am Hornbachjoch sowie nördlich des Großen Wilden bis südöstlich der Schönberghütte und westlich des Kreuzkopfes aufgeschlossen. Sie ist messerscharf ausgebildet und fällt überwiegend flach nach Süd bis Südsüdost ein. Direkt unter der Deckengrenze treten obertriassische Hauptdolomit-Schürflinge der Lechtal-Decke in der überfahrenen, völlig zerscherten, unterjurassischen Allgäu-Formation der Allgäu-Decke auf, wobei Hartbänke vielfach intensiv in Phacoide zerlegt sind. Die Allgäu-Formation ist aber nicht überall deckenparallel, sondern kann durchaus auch von unten stumpfwinkelig bis nahezu senkrecht gegen die Deckengrenze stossen. Die flachen Deckenüberschiebungen nehmen aber nur im wenigsten der Fälle einen geradlinigen, sondern zeigen meist einen gezackten Verlauf. Ein gutes Beispiel ist die Überfahrung der Lechtal-Decke nördlich des Litnisschrofens, die starke Richtungsänderungen und auch sehr veränderliche Einfallswerte aufweist. Dies ist sowohl durch den strukturgeologischen Aufbau der unterlagernden Algäu-Decke als auch durch Blattverschiebungen quer zur Überschiebungsrichtung zu erklären. Die Überschiebungen können aber auch sehr steil erfolgen, wie dies im Süden der Luitpoldzone zu sehen ist und generell entlang des gesamten Nordrandes der Allgäu-Decke
Base of the Lechtal Nappe
Base of the Lech Valley Nappe
Basis der Lechtal-Decke
The base of the Krabachjoch Nappe of the Tirolic-Noric Nappe System lies north of St.Anton/Arlberg and west of Imst.
Die Basis der Krabachjoch-Decke des Tirolisch-Norischen Deckensystems ist nördlich von St. Anton am Arlberg, sowie westlich von Imst zu finden. (May & Eisbacher, 1999)
Basis der Krabachjoch-Decke
Base of the Krabachjoch Nappe
The base of the Totes Gebirge Nappe of the Tirolic-Noric Nappe System lies between north of Altaussee and west of Steyrling.
Die Basis der Totes Gebirge-Decke des Tirolisch-Norischen Deckensystems kann von nördlich von Altaussee bis welstlich vom Steyrling verfolgt werden.
Basis der Totes Gebirge-Decke
Base of the Totes Gebirge Nappe
The base of the Berchtesgarden Nappe of the Juvavic Nappe System can be followed in Austria along the German-Austrian border from east of Wildental via the Saalach Valley to east of Unken.
Basis der Berchtesgaden-Decke
Base of the Berchtesgaden Nappe
Die Basis der Berchtesgaden-Decke des Juvavischen Deckensystem kann in Österreich entlang der Grenze zu Deutschland von östlich von Wildental, über das Saalachtal bis östlich von Unken verfolgt werden.
The base of the Pusterwald Nappe, a lower nappe of the Koralpe-Wölz Nappe System is represented at map sheets of the Geological Survey of Austria (Moser, 2015; Ebner et al., 2017; Iglseder, 2019). The emplacement took place during the Eoalpine orogenesis.
Die Basis der Saualpe-Koralpe-Decke, einer liegenden Einheit des Koralpe-Wölz-Deckensystems ist teilweise auf Karten der Geologischen Bundesanstalt dargestellt (Moser, 2015; Ebner et al., 2017; Iglseder, 2019). Ihre Platznahme erfolgte während der eoalpidischen Gebirgsbildung (Schuster, 2015).
Base of the Saualpe-Koralpe Nappe
Basis der Saualpe-Koralpe-Decke
The base of the Reichraming Nappe of the Bajuvaric Nappe System can be followed from north of Molln in the west to north of Reichraming in the east.
Die Basis der Reichraming-Decke des Bajuvarischen Deckensystems kann von nörldich von Molln im Westen bis nördlich von Reichraming im Osten verfolgt werden.
Basis der Reichraming-Decke
Base of the Reichraming Nappe
The base of the Silvretta-Seckau Nappe System seperates the Upper Austroalpine from the Lower Austroalpine. It can be observed in Austria in the south of Vorarlberg and Tirol (?), in the Tauern Window in the area between Flachau and Mauterndorf, and between the Mürz Valley and St. Lorenzen/Wechsel. The Nappe Stystem is overlain by the Greywacke Zone and Koralpe-Wölz Nappe Systems (Froitzheim et al., 2008).
Die Basis des Silvretta-Seckau-Deckensystems trennt das Oberostalpin vom Unterostalpin. Sie ist im Süden von Tirol und Vorarlberg zu finden, im Tauernfenster zwischen Flachau und Mauerndorf, sowie zwischen Mürztal und St. Lorenzen am Wechsel. Das Deckensystem wird vom Grauwackenzone-Deckensystem und vom Koralpe-Wölz-Deckensystem überlagert (Froitzheim et al., 2008).
Base of the Silvretta-Seckau Nappe System
Basis des Silvretta-Seckau-Deckensystems
The base of the Rhenodanubian Nappe System can be observed in Austria and Germany along the north of the Eastern Alps - from the norhern part of Vorarlberg via north of Salzburg to northwest of Vienna. The cretaceous to eocene sediments were stacked in several nappes beneath the Austroalpine through N–NW oriented overthrusting (Froitzheim et al., 2008).
Die Basis des Rhenodanubischen Deckensystems kann im Norden der Ostalpen in Österreich und Deutschland von Vorarlberg über nördlich von Salzburg bis nordwestlich von Wien beobachtet werden. Die kreidezeitlichen bis eozänen Sedimente wurden durch N–NW-gerichtete Überschiebungen in mehreren Decken in einem Akkretionskeil unter dem Ostalpin gestapelt (Froitzheim et al., 2008).
Base of the Rhenodanubian Nappe System
Basis des Rhenodanubisches Deckensystems
The base of the Laufnitzdorf Nappe can be observed between west of Großstübing and south of Schrems.
Die Basis der Laufnitzdorf-Decke kann zwischen westlich von Großstübing und südlich von Schrems beobachtet werden.
Base of the Laufnitzdorf Nappe
Basis der Laufnitzdorf-Decke
The NW-SE striking and SW-dipping base of the Exenberg Nappe extends from Stanz im Mürztal to just west of Rossegg. For most its extend, it corresponds also to the base of the Koralpe-Wölz Nappe System, except for short part west of the Lindkogel, where it is thrusted over the Radegund Nappe
Die NW-SE streichende und nach SW eintauchende Basis der Exenberg-Decke ist zwischen Stanz im Mürztal und Rossegg aufgeschlossen. Größtenteils entspricht diese Deckenbasis der Basis des Koralpe-Wölz-Deckensystems, außer für einen kurzen Bereich westlich des Lindkogels, wo die Exenberg-Decke über die Radegund-Decke geschoben wurde.
Base of the Exenberg Nappe
Basis der Exenberg-Decke
The base of the Ultrahelveticum can in Austria mainly be found in Vorarlberg between Feldkirch and Hirschegg, but also between Gresten and Texingtal in Lower Austria. The Ultrahelveticum was overthrust onto the Helveticum sensu stricto during the Oligocene and was itself integrated into the nappe structure by the later principal overthrust (out-of-sequence) of the Helvetic nappes (Froitzheim et al., 2008).
Die Basis des Ultrahelvetikums ist in Österreich hauptsächlich in Vorarlberg zwischen Feldkirch und Hirschegg aufgeschlossen, aber auch zwischen Gresten und Texingtal in Niederösterreich. Das Ultrahelvetikum wird im Oligozän auf das Helvetikum s.str. überschoben und wird durch die spätere Hauptüberschiebung (out-of-sequence) der Helvetischen Decken selbst in den Deckenbau einbezogen (Froitzheim et al., 2008).
Base of the Ultrahelvetic Units
Basis des Ultrahelvetikums
The base of the Dachstein Nappe of the Juvavic Nappe System crops out in the Ramsau area between Sulzbach and Untersee, and from east of Archkogel at the Lake Grundlsee to the Tauplitzalm.
Basis der Dachstein-Decke
Base of the Dachstein Nappe
Die Basis der Dachstein-Decke des Juvavischen Deckensystem ist in der Ramsau zwischen Sulzbach und Untersee aufgeschlossen, sowie östlich von Archkogel am Grundlsee bis zur Tauplitzalm.
The base of the uppermost nappe system of the Moldanubian Nappes can in Austria be observed in Lower Austria, between Ybbs/Donau and Raabs/Thaya. The Gföhl Nappe System overthrusts the Drosendorf Nappe System and the Ostrong Nappe System.
Die Basis des obersten Deckensystems des Moldanubikums ist in Österreich nur in Niederösterreich, zwischen Ybbs and der Donau und Raabs an der Thaya zu finden. Das Gföhl-Deckensystem überfährt an seiner Basis das Drosendorf-Deckensystem bzw. das Ostrong Deckensystem.
Base of the Gföhl Nappe System
Basis des Gföhl-Deckensystems
The emplacement the Gstoder Nappe, an upper nappe of the Koralpe-Wölz Nappe System, took place during the Eoalpine ogogenesis. Earlier shear zones are overprinted by later top-E-directed structures (Iglseder, 2019; Iglseder & Huet, 2019 and references therein; Rantitsch et al., 2020).
Die Platznahme der Gstoder-Decke, eine der hangenden Decken des Koralpe-Wölz-Deckensystems, erfolgte während der eoalpidischen Gebirgsbildung. Dabei wurden frühere Scherzonen von späteren top-E-gerichteten Strukturen überprägt (Iglseder, 2019; Iglseder & Huet, 2019 und die darin aufgeführten Referenzen; Rantitsch et al., 2020).
Base of the Gstoder Nappe
Basis der Gstoder-Decke
The base of the Pusterwald Nappe, a lower nappe of the Koralpe-Wölz Nappe System is represented at map sheets of the Geological Survey of Austria (Metz, 1979; Moser, 2015; Ebner et al., 2017; Iglseder, 2019). The emplacement took place during the Eoalpine orogenesis.
Die Basis der Pusterwald-Decke, einer liegenden Einheit des Koralpe-Wölz-Deckensystems ist teilweise auf Karten der Geologischen Bundesanstalt dargestellt (Metz, 1979; Moser, 2015; Ebner et al., 2017; Iglseder, 2019). Ihre Platznahme erfolgte während der eoalpidischen Gebirgsbildung (Schuster, 2015).
Basis der Pusterwald-Decke
Base of the Pusterwald Nappe
The base of the Hochlantsch Nappe, an upper nappe of the Drauzug-Gurktal Nappe System is represented at map sheets of the Geological Survey of Austria (Flügel et al., 1990; Ebner et al., 2017). The emplacement took place during the Eoalpine orogenesis.
Die Basis der Hochlantsch-Decke, einer hangenden Decke des Drauzug-Gurktal-Deckensystems ist teilweise auf Karten der Geologischen Bundesanstalt dargestellt (Flügel et al., 1990; Ebner et al., 2017). Ihre Platznahme erfolgte während der eoalpidischen Gebirgsbildung (Fritz, 1988).
Base of the Hochlantsch Nappe
Basis der Hochlantsch-Decke
The base of the Schöckel Nappe, an upper nappe of the Drauzug-Gurktal Nappe System is represented at map sheets of the Geological Survey of Austria (Flügel et al., 1990, 2011; Ebner et al., 2017). The emplacement took place during the Eoalpine orogenesis.
Die Basis der Schöckel-Decke, einer hangenden Decke des Drauzug-Gurktal-Deckensystems ist teilweise auf Karten der Geologischen Bundesanstalt dargestellt (Flügel et al., 1990; Ebner et al., 2017). Ihre Platznahme erfolgte während der eoalpidischen Gebirgsbildung (Fritz, 1988).
Base of the Schöckel Nappe
Basis der Schöckel-Decke
The emplacement of the Stolzalpe Nappe of the Drauzug-Gurktal Nappe System took place during Cretaceous Eoalpine nappe stacking and shows WNW-directed kinematics. This was reactivated at ESE-directed normal faults, localized at the underlying Königstuhl- and Bundschuh nappes (Iglseder, 2019; Iglseder & Huet, 2019 and references therein; Rantitsch et al., 2020).
Die Platznahme der Stolzalpe-Decke des Drauzug-Gurktal-Deckensystem erfolgte während der Eoalpidischen (kretazischen) Deckenstapelung als Überschiebungen mit WNW-gerichteter Bewegung. Diese wurde von ESE-gerichteten Abschiebungen, lokalisiert an der Deckengrenze zur Königstuhl- und Bundschuh-Decke, reaktiviert (Iglseder, 2019; Iglseder & Huet, 2019 und die darin aufgeführten Referenzen; Rantitsch et al., 2020).
Basis der Stolzalpe-Decke
Base of the Stolzalpe Nappe
In the Eastern Alps, the Helveticum sensu stricto (and its base) only occurs west of Salzburg. At about 30 Ma, the 'out-of-sequence' overthrusting of the Helvetic Nappes formed through the emplacement on the Infra-Helveticum and the Sub-Alpine Molasse, which continued into the Miocene (Pfiffner, 2009).
In den Ostalpen kommt das Helvetikum sensu stricto, und damit auch dessen Basis, nur westlich von Salzburg vor. Um ca. 30 Ma bildeten sich die 'out-of-sequence'-Überschiebungen der Helvetischen Decken mit der Platznahme auf dem Infrahelvetikum und der Subalpinen Molasse, die bis ins Miozän andauerten (Pfiffner, 2009).
Basis des Helvetikums sensu stricto
Base of the Helvetic Nappes
The emplacement of the Königstuhl Nappe of the Drauzug-Gurktal Nappe System overthrusting the Ackerl, Murau, Pfannock and Bundschuh Nappes took place during Cretaceous Eoalpine nappe stacking with WNW-directed movement. Later normal-faulting with top ESE-directed kinematics overprinted these nappe boundaries (Iglseder, 2019; Iglseder & Huet, 2019 and references therein; Rantitsch et al., 2020).
Die Platznahme der Königstuhl-Decke des Drauzug-Gurktal-Deckensystem, welche die Pfannock-, Ackerl-, Murau- sowie die Bundschuh-Decke überlagert, erfolgte während der eoalpidischen Gebirgsbildung. Die Deckengrenzen zeigen Überschiebungen mit top-WNW-gerichteter Kinematik, welche durch spätere ESE-gerichtete Abschiebungen überprägt werden (Iglseder, 2019; Iglseder & Huet, 2019 und die darin aufgeführten Referenzen; Rantitsch et al., 2020).
Basis der Königstuhl-Decke
Base of the Königstuhl Nappe
The base of the Ackerl Nappe of the Drauzug-Gurktal Nappe System overthrusting the Murau and Stolzalpe Nappes can be observed south of St. Lorenzen ob Murau and took place during Eoalpine orgenesis. Earlier NW-directed structures are overprinted by later top (E)SE-directed ones (Iglseder, 2019; Iglseder & Huet, 2019 and references therein; Rantitsch et al., 2020).
Die Basis der Überschiebung der Ackerl-Decke des Drauzug-Gurktal-Deckensystem auf die Murau- und Stolzalpe Decken ist südlich St. Lorenzen ob Murau aufgeschlossen und wurde während der eoalpidischen Gebirgsbildung angelegt. Diese zeigen frühere NW-gerichtete Strukturen welche von späteren top-(E)SE-gerichteten überprägt werden (Iglseder, 2019; Iglseder & Huet, 2019 und die darin aufgeführten Referenzen; Rantitsch et al., 2020).
Basis der Ackerl-Decke
Base of the Ackerl Nappe
The base of the Murau Nappe of the Drauzug-Gurktal Nappe System overthrusting basal nappes of the Drauzug-Gurktal Nappe System as well as nappes of the Koralpe-Wölz and Ötztal-Bundschuh Nappe Systems was activated during Eoalpine nappe stacking with partly top-W-directed kinematics. Later structures with top-E-directed shearing overprint this boundary (Iglseder, 2019; Iglseder & Huet, 2019 and references therein; Rantitsch et al., 2020).
Die Basis der Überschiebung der Murau-Decke des Drauzug-Gurktal-Deckensystem auf basale Decken des Drauzug-Gurktal-Deckensystems, sowie das Koralpe-Wölz- und Ötztal-Bundschuh-Deckensystem wurde während der eoalpidischen Deckenstapelung angelegt und zeigt teilweise top-W-gerichtete Kinematik. Dies wurden von späteren Strukturen mit top-E-gerichteter Scherung überprägt (Iglseder, 2019; Iglseder & Huet, 2019 und die darin aufgeführten Referenzen; Rantitsch et al., 2020).
Base of the Murau Nappe
Basis der Murau-Decke
On the western side of the Wechselfenster, the Stuhleck-Kirchberg Nappe features a Cretaceous contact dipping gently towards west on top of the Vorau Nappe (Silvretta-Seckau Nappe System) and Wechsel Nappe (Lower Austroalpine Nappes). Similar situation can be spotted on the western side of the Wiesmath Fenster where the contact zone inclines WSW. The formation of the base of the Stuhleck-Kirchberg Nappe next to the Rechnitzer Fenster group (part of the Penninic Nappe) was originated during Miocene by steeply ENE dipping normal faults.
An der Westseite des Wechselfensters zeigt die Stuhleck-Kirchberg-Decke einen flach gegen Westen fallenden kretazischen Kontakt zur unterlagernden Vorau-Decke des Silvretta-Seckau-Deckensystems und zur Wechsel-Decke des Unterostalpins. Auch an der Westseite des Wiesmather Fensters ist eine flach, WSW fallende kretazische Deckengrenze erhalten. Die Deckengrenzen gegenüber den Penninischen Decken im Bereich der Rechnitzer Fenstergruppe und Begrenzungen, die durch steilstehende, oft gegen ENE einfallende Abschiebungen gebildet werden, entstanden im Miozän.
Basis der Stuhleck-Kirchberg-Decke
Base of the Stuhleck-Kirchberg Nappe
The emplacement of the Sieggraben Nappe took place in the Upper Cretaceous and is caused by a NE-dipping thrust fault. The remnants of the thrust fault are exposed between Pinkafeld and Mattersburg, east of the area of the Hochwechsel and at the eastern margin of the Bucklige Welt. The primary contact has been reworked by younger faults.
Die Platznahme der Sieggraben-Decke erfolgte an einer NE gerichteten Überschiebung in der Oberkreide. Die heute noch erhaltenen Teile der Überschiebung finden sich zwischen Pinkafeld und Mattersburg östlich des Hochwechsels bzw. am östlichen Rand der Buckligen Welt. Die primären Kontakte sind lokal durch steilstehende jüngere Störungen überprägt.
Basis der Sieggraben-Decke
Base of the Sieggraben Nappe
The base of the Frankenfels Nappe of the Bajuvaric Nappe System can be observed between Maria Neustift in the north and St. Gallen in the south.
Die Basis der Frankenfels-Decke des Bajuvarischen Deckensystems ist zwischen Maria Neustift und St. Gallen im Süden beobachten.
Base of the Frankenfels Nappe
Basis der Frankenfels-Decke
The base of this unit of the Rhenodanubic Nappe System in the Wienerwald can be observed in the area of Wöllersdorf.
Diese tektonische Einheit des Rhenodanubikums kann bei Wöllersdorf beobachtet werden.
Basis der Laab-Decke
Base of the Laab Nappe
The base of the Hallstatt Nappe of the Juvavic Nappe System can be observed west of Lake Hallstatt and east of Johnsbach.
Die Basis der Hallstatt-Decke des Juvavischen Deckensystems kann westlich vom Hallstätter See und östlich von Johnsbach beobachtet werden.
Base of the Hallstatt Nappe
Basis der Hallstatt-Decke
This nappe of the Rhenodanubian Nappe System is the dominating tectonic unit of the Flysch Zone in Lower Austria and the Wienerwald. The base of the Greifenstein Nappe can be observed between Kettenreith in the southwest and St. Andrä-Wördern in the northeast.
Diese Decke des Rhenodanubikums ist die dominierende tektonische Einheit in der Flyschzone Niederösterreichs bzw. des Wienerwaldes. Die Basis der Greifenstein-Decke kann zwischen Kettenreith im Südwesten und St. Andrä-Wördern im Nordosten beobachtet werden.
Basis der Greifenstein-Decke
Base of the Greifenstein Nappe
The base of the Göller Nappe is a subhorizontal S-dipping thrust fault that stretches from the Salza Valley in the SW via Lake Erlauf (north of Mariazell) across the Vienna Basin in the NE. Just West of the Vienna Basin, it conincides with the nappe boundary between the hanging Tirolic-Noric Nappe System and its footwall, the Bajuvaric Nappe System
Die Basis der Göllerdecke ist eine subhorizontale, nach S einfallende Überschiebung, die vom Salzatal im SW über den Erlaufsee (N von Mariazell) bis zum Untergrund des Wiener Beckens verläuft. Westlich des Wiener Beckens entspricht die Basis der Göller-Decke auch der Deckengrenze zwischen dem hangenden Tirolisch-Norischen und dem liegenden Bajuvarischen Deckensystem.
Base of the Göller Nappe
Basis der Göller-Decke
The base of the Unterberg Nappe is a subhorizontal, S-dipping thrust fault that stretches from the village of Mooslandl in the Enns River Valley in the SW to Altenmark an der Triesting in the NE.
Die Basis der Unterberg-Decke ist eine subhorizontale, nach S einfallende Überschiebung, die von Mooslandl im Ennstal im SW bis Altenmark an der Triesting im NE verfolgbar ist.
Base of the Unterberg Nappe
Basis der Unterberg-Decke
This Juvavic nappe and its base can be observed in the area of the Schneeberg between Gußwerk and Naßwald.
Diese Juvavische Decke, sowie ihre Basis sind im Schneeberggebiet zwischen Gußwerk und Naßwald zu finden.
Basis der Schneeberg-Decke
Base of the Schneeberg Nappe
The base of the Reisalpe Nappe of the Tirolic-Noric Nappe System is a subhorizontal S-dipping thrust fault that stretches from Lake Lunz in the SW to Pankraziberg in the NE. In large parts, it conincides with the nappe boundary between the hanging Tirolic-Noric Nappe System and its footwall, the Bajuvaric Nappe System
Die Basis der Reisalpe-Decke des Tirolisch-Norischen Deckensystems ist eine subhorizontal nach S einfallende Überschiebung, die vom Lunzer See im SW bis Pankraziberg im NE verfolgbar ist. In großen Teilen entspricht sie der Deckengrenze zwischen dem hangenden Tirolisch-Norischen und dem liegenden Bajuvarischen Deckensystem.
Base of the Reisalpe Nappe
Basis der Reisalpe-Decke
This Bajuvaric nappe and its base can be observed southwest of Vienna in the area the Föhrenberge nature park south of Kaltenleutgeben.
Diese Bajuvarische Decke und ihre Basis ist im Südwesten von Wien Naturpark Föhrenberge südlich von Kaltenleutgeben zu beobachten.
Basis der Lunz-Decke
Base of the Lunz Nappe
This nappe system comprises the lowermost nappes of the Greywacke Zone Nappe System, overthrusting the Silvretta-Seckau Nappe System at its base, which only crops out in the area of Großstübing and Deutschfeistritz. (Neubauer, 1994).
Dieses Deckensystem umfasst die untersten Decken der Grauwackenzone, es überschiebt an seiner Basis, welche nur um Großstübing und Deutschfeistritz aufgeschlossen ist, das Silvretta-Seckau-Deckensystem (Neubauer, 1994; Schuster, 2015).
Basis des Veitsch-Silbersberg-Deckensystems
Base of the Veitsch-Silbersberg Nappe System
This fault set consists of faults within the Austrian part of the Lower Bavarian - Upper Austria Molasse Basin between Salzburg in the west and Melk in the east. It is bound by the outcropping crystalline rock suites of the Bohemian Massif to the north and northeast, and the Alpine Thrust front to the south. All faults within the basin are blind faults, active until Badenian of mid-Miocene at the latest, solely evidenced by seismic surveys and drillings. (Kröll et al., 2001; Wagner, 1998)
Dieses Störungset besteht aus Störungen des österreichischen Teils des Unterbayrisch-oberösterreichischen Mollassebeckens zwischen Salzburg im Westen und Melk im Osten. Es wird im Norden und Nordosten von Kristallingesteinen der Böhmischen Masse begrenzt und von der Alpinen Überschiebungsfront im Süden. Alle Brüche innerhalb des Beckens sind blinde Störungen, die längstens bis ins Baden des Mittleren Miozäns aktiv waren, und die nur mittels Seismik und Bohrungen nachgewiesen wurden. (Kröll et al., 2001; Wagner, 1998)
West Molasse Fault Set
Westliche Molasse Störungsset
Überdeckte, E-W streichende, steil N-fallende Störung an der Basis des Molassebeckens, Zweig der Aspach Störung [AT_10662], der sich im Osten bis nach Pudexing (AT) zieht.
This E-W striking, steeply N-dipping blind fault at the bottom of the Molasse Basin represents a branch of the Aspach Fault [AT-10662] and terminates to the east near Pudexing (AT).
Roith Fault
Roith-Störung
Überdeckte E-W streichende, steil nach N einfallende Störung an der Basis des Molassebeckens als Zweig der Altheim Störung [AT-10661] der sich bis östlich von Braunau (AT) zieht
Aselkam-Störung
This E-W striking, steeply N-dipping blind fault at the bottom of the Molasse Basin represents a branch of the Altheim Fault [AT-10661] and terminates to the east in the city of Braunau (AT).
Aselkam Fault
W-E striking, vertical to steeply S-dipping blind normal fault at the bottom of the Molasse Basin representing the northern branch of the Nonsbach Fault [AT-10657] and terminating to the east of the city of Braunau (AT). Target of Simbach-Braunau geothermal development
Überdeckte, W-E streichende, vertikale bis steil S-fallende Abschiebung an der Basis des Molassebeckens als Nord-Ast der Nonsbach Störung [AT_10657] der sich bis östlich von Braunau (AT) zieht. Ziel des Simbach-Braunau Geothermie-Vorhabens.
Altheim-Störung
Altheim Fault
Überdeckte ENE-WSW streichende, N-fallende Störung an der Basis des Molassebeckens die sich im Osten bis zum Deggendorf-Ried Störungssystem [DE-BY_929] bei Mehrnbach (AT), im Westen bis zum Landshut-Neuötting Abbruch zieht.
Aspach Störung
Aspach Fault
This ENE-WSW striking, N-dipping blind fault at the bottom of the Molasse Basin terminates in the east at the Deggendorf-Ried Fault close to Mehrnbach (AT) and in the west at the Landshut-Neuötting Fault System.
Aspach-Störung
This ENE-WSW striking, N-dipping blind fault at the bottom of the Molasse Basin terminates in the east at the Deggendorf-Ried Fault System [DE-BY_929] close to Mehrnbach (AT) and in the west at the Landshut-Neuötting Step Fault.
Landshut-Neuötting Fault System
This fault system comprises the NW-SE striking faults, which limit the Landshut-Neuöttinger Hoch. They can be traced from Landshut (D) via Neuötting (D) and Burghausen to the northern rim of the Alps near Michaelbeuren, Perwang and Berndorf north of Salzburg. (Buchroithner, 1984; Unger & Schwarzmeier, 1982; Scheck-Wenderoth et al., 2008)
Dieses Störungssystem umfasst die NW-SE streichenden Störungen, die das Landshut-Neuöttinger Hoch begrenzen und lassen sich von Landshut (D) über Neuötting (D) und Burghausen bis zum Alpennordrand bei Michaelbeuren, Perwang und Berndorf nördlich von Salzburg verfolgen. (Buchroithner, 1984; Unger & Schwarzmeier, 1982; Scheck-Wenderoth et al., 2008)
Landshut-Neuötting-Störungssystem
Mehring-Seeham Fault
Mehring-Seeham Störung
Southwestern branch of the continuation of Landshut-Neuötting Fault Scarp 2 [DE-BY_702], branching off Eggelsbach Fault [AT_10663] just north of the Austrian border. NW-SE trending, on average approx. 75° SW dipping normal fault forming an intermediate step SW of Fault Scarp 2 along the Central Swell Zone in Austria.
Als Abzweig der Landshut-Neuötting Abbruchstufe 2 [DE-BY_702] wenig nördlich der österreichischen Grenze, zieht sich diese NW-SE verlaufende, im Mittel ca. 75° nach SW einfallende Abschiebung, unter Bildung einer Zwischenstufe SW vor der Abbruchstufe 2, entlang der Zentralen Schwellenzone bis zum Obertrumer See.
Grasset-Wechselberg Fault
Landshut-Neuötting Abbruchstufe 4
Grasset-Wechselberg Störung
Running from south of Altötting into Austrian territory, southwestward arcuate, NW-SE trending, approx. 75° NE dipping reverse fault featuring a cumulative throw of up to 450 m. Southwestern boundary of the protrusion of the lower step of Landshut-Neuötting Rise overthrusting the southern part of Gifthal Trough.
Südwestwärts gebogene, NW-SE verlaufende, ca. 75° nach NE einfallende Haupt-Aufschiebung (begleitet von kleineren Aufschiebungen) mit einem kumulativen Versatz von bis zu 450 m, die sich von südlich Altötting bis nach Franking in Österreich zieht. Südwestgrenze des Vorsprungs der unteren Stufe des Landshut-Neuötting Abbruchs, der die südlichen Ausläufer des Gifthal Trogs überfahren hat.
Südöstliche Fortsetzung des Landshut-Neuötting Hauptabbruchs [DE-BY_701]. Steil nach SW einfallende Abschiebung die als überdeckte Störung an der Basis des Molassebeckens von nördlich Burghausen (DE) südost- bis ostwärts bis zur Ried Störung [AT_10665] westlich von Neukirchen an der Vöckla (AT) verläuft.
This SW-dipping blind fault at the bottom of the Molasse Basin marks the northeastern border of the Landshut-Neuötting Fault System and can be traced from north of Burghausen (D) towards SE until the west of Neukirchen an der Vöckla (AT), where it terminates at the Deggendorf-Ried Fault
Diese nach SW einfallende blinde Störung an der Molassebasis markiert die nordöstliche Grenze des Landshut-Neuötting Störungsystems, und kann von nördich von Burghausen (D) nach SE hin bis westlich von Neukirchen and er Vöckla (AT) verfolgt werden, wo es von der Deggendorf-Ried-Störung abgeschnitten wird.
Handenberg Störung
Southeastern continuation of Landshut-Neuötting Main Scarp [DE-BY_701] this steeply SW-dipping blind fault at the bottom of the Molasse Basin can be traced from north of Burghausen (DE) towards SE until the west of Neukirchen an der Vöckla (AT), where it terminates at the Ried Fault [AT_10665].
Handenberg Fault
Northeastern branch of the continuation of Landshut-Neuötting Fault Scarp 2 [DE-BY_702], this SW-dipping blind fault at the bottom of the Molasse Basin runs through Burghausen (DE) towards SE via Perwang am Grabensee (AT) and Neumarkt am Wallersee (AT) and terminates at lake Irrsee.
Als nordöstlicher Ast der Fortsetzung der Landshut-Neuötting Abbruchstufe 2 [DE-BY_702], verläuft diese überdeckte, im Mittel ca. 75° nach SW einfallende synthetische Abschiebung an der Basis des Molassebeckens von Mehring NW Burghausen (DE) südostwärts via Perwang am Grabensee (AT) und Neumarkt am Wallersee (AT) bis zum Irrsee.
This SW-dipping blind fault at the bottom of the Molasse Basin runs through Burghausen (D) towards SE via Perwang am Grabensee (AT) and Neumarkt am Wallersee (AT) and terminates at lake Irrsee.
Die nach SW einfallende blinde Störung an der Basis des Molassebeckens verläuft durch Burghausen (D) in Richtung SE über Perwang am Grabensee (AT) und Neumarkt am Wallersee (AT) und endet am Irrsee.
Eggelsbach Fault
Eggelsbach Störung
Geinberg-Simbach Störung
Überdeckte, E-W streichende, ca. 70° nach N einfallende Abschiebung an der Basis des Molassebeckens zwischen N von Geinberg (AT) und Bertenöd NE Simbach (DE); quert den Inn (Deutsch-Österreichische Grenze) bei Mining (AT). Ziel des Geothermie-Vorhabens Geinberg
W-E striking, approx. 70° N dipping blind normal fault at the bottom of the Molasse Basin is located to the north of Geinberg (AT) and northeast of Simbach (DE) and crossing the Inn River (Austria-German border) at Mining (AT). Target of Geinberg geothermal development.
Geinberg-Simbach-Störung
Geinberg-Simbach Fault
Fornach Störung
Fornach Fault
Fornach-Störung
This SE-NW striking, steeply NE dipping blind fault at the bottom of the Molasse Basin terminates in the SE at the Landshut-Neuötting fault System close to Fornach (AT) and towards the NE near the town of Wagham (AT)
Diese SE-NW-streichende, steil nach NE einfallende blinde Störung an der Basis des Molassebeckens verläuft von SE, wo sie vom Landshut-Neuötting-Störungssystem nahe Fornach (AT) abgeschnitten wird, Richtung NE nahe Wagham (AT)
Branching off southwardly from Danube Fault Scarp [DE-BY_698], a N-S to NW-SE trending fault system of approx. 70° to 80° W to SW dipping normal faults runs from Deggendorf to Ried in Upper Austria the subsurface of the Alpine Molasse Eastern boundary of the Molasse Basin towards the Aidenbach-Griesbach Rise (resp. the Osterhofen pre-rise) featuring a thin sequence of fluviatile Molasse sediments only. The NNE-SSW striking fault runs at subsurface from Deggendorf (D) via Ried im Innkreis towards the Attersee. It is only confirmed by seismic and borehole data. (Freudenberger & Schwerd, 1996; Kröll et al., 2006)
Südlicher Abzweig vom Donaurandbruch [DE-BY_698], N-S bis NW-SE verlaufendes System, ca. 70° bis 80° nach W bis SW einfallender Abschiebungen zwischen Deggendorf und Ried in Oberösterreich. Östliche Grenze des Molassebeckens zum Aidenbach-Griesbach Hoch hin (bzw. zur Osterhofen Vorstufe), das nur geringermächtige fluviatile Molassesedimente aufweist. Dieses NNE-SSW streichende, im Molasseuntergrund von Deggendorf (D) über Ried im Innkreis bis zum Attersee verlaufende Störungssystem ist nur durch Seismik- und Bohrlochdaten belegt. (Freudenberger & Schwerd, 1996; Kröll et al. 2006)
Deggendorf-Ried Faultsystem
The tectonic boundaries of the Deggendorf-Ried Faultsystem largely are blind faults 3D modelled based on evidence of seismic and gravity surveys and deep drillings. The concepts refer to the fault traces at the top surface of Upper Jurassic carbonate sequence (restricted to the hanging wall in large areas), one of the principal reflectors in seismic surveys. Tectonic boundaries featuring throws of less than approximately 10 m, likewise soft links between faults, like relay ramps or horsetail splays, commonly are subseismic in legacy surveys and detectable only in novel 3D-seismics, so far not carried out in the area. The inventory, thus, cannot be complete with respect to these features, reflects the state of knowledge as of 2020 and is subject to future amendments.
Die tektonischen Grenzflächen des Deggendorf-Ried Störungssystem sind größtenteils überdeckte Störungen, die im 3D-Modell aus seismischen und Schwere-Messungen sowie Bohrungsbelegen abgeleitet wurden. Die Konzepte der tiefliegenden Störungen beziehen sich auf die im 3D-Modell ermittelten Schnittspuren an der Oberfläche der Liegendscholle, d.h. der Weißjura Karbonat-Abfolge, wobei dessen Vorkommen oft auf die Tiefscholle beschränkt ist. Tektonische Grenzflächen mit Sprunghöhen von weniger als ca. 10 m, oder Übergänge zwischen Störungen wie Akkomodationszonen (relay ramps) oder Auffiederungen (horsetail splays), sind in älteren seismischen Erkundungen gemeinhin nicht erkennbar (subseismisch) und nur in moderner, im Gebiet bisher nicht durchgeführter 3D-Seismik identifizierbar. Dementsprechend bleibt die Zusammenstellung, Stand 2020, im Hinblick auf solche Phänomene unvollständig und ist Gegenstand künftiger Fortschreibungen.
Deggendorf-Ried Störungssystem
Pocking Step Fault
Pockinger Abbruch
Northeastern branch of southern continuation of the Aidenbach-Griesbach Step Fault. Blind, undulate NW-SE trending, approx. 80° SW dipping multiphase normal fault featuring a throw of up to 1 km.
Nordöstlicher Zweig der südlichen Fortsetzung des Aidenbach-Griesbach Abbruchs. NW-SO verlaufende, ca. 80° nach SW einfallende mehrphasige Abschiebung mit einer Sprunghöhe von bis zu 1 km.
Osterhofen Frontal Scarp
Osterhofener Abbruch
N-S to NNW-SSE trending, approx. 70° ± W dipping normal fault, side branch of Aidenbach-Griesbach Step Fault representing the western boundary of the Osterhofen prestage of the Aidenbach-Griesbach Rise.
N-S to NNW-SSE verlaufende, ca. 70° nach ± W einfallende Abschiebung. Seitenast des Aidenbach-Griesbach Abbruchs und westliche Begrenzung der Osterhofen Vorstufe zum Aidenbach-Griesbach Hoch.
Winklarn-Pörndorf Subfault
Winklarn-Pörndorf Nebenstörung
NNW-SSE trending, approx. 80° WSW dipping synthetic normal fault; branch of Osterhofen Frontal Scarp [DE-BY_1241].
NNW-SSO verlaufende, ca. 80° nach WSW einfallende synthetische Abschiebung, Zweig des Osterhofen Abbruchs [DE-BY_1241].
Aidenbach-Griesbach Step Fault
Schwaimer Abbruch
Aidenbach-Griesbach Abbruch
Northern section of Deggendorf-Ried Fault System, linked by a relay structure to the Pocking Step Fault [DE-BY_669] in the south. Blind N-S to NNW-SSE trending, on average approx. 80° W to WSW dipping, multiphase normal fault, in large parts step fault, featuring a cumulative throw of up to more than 1 km.
Nördlicher Abschnitt des Deggendorf-Ried Störungssystems, im Süden durch eine Relay-Struktur mit dem Pockinger Abbruch [DE-BY_669] verbunden. Nicht aufgeschlossene N-S bis NNW-SSO verlaufende, im Durchschnitt ca. 80° nach W bis WSW einfallende, großteils gestaffelte, mehrphasige Abschiebung mit einer kumulativen Sprunghöhe bis über 1 km.
Brand-Dobelwiese Fault
Displacing Paleo-Donaurand Fault Scarp [DE-BY_1237], SW-NE striking, steeply NW dipping double normal fault, southeastern border of the Flintsbach Jurassic carbonates trough-like embayment into the marginal Bohemian Massif crystalline rock suites.
Brand-Dobelwiese Störung
SW-NE streichende, steil nach NW einfallende Doppel-Abschiebung als südöstliche Grenze der Flintsbacher Jurakalk-Bucht in den Kristallingesteinen am Rand der Böhmischen Masse und versetzt den Paläo-Donaurandbruch [DE-BY_1237].
Flintsbach Fault
Flintsbach Störung
Slight westward arcuate SW-NE trending, approx. 80° NW dipping normal fault, northwestern border of the Flintsbach Jurassic carbonates trough-like embayment into the marginal Bohemian Massif crystalline rock suites, offsetting Paleo-Donaurand Fault Scarp [DE-BY_1237]. Merges into Aidenbach-Griesbach Step Fault [DE-BY_764] forming the western boundary of a downthrow block featuring Jurassic carbonates at shallow depth.
Leicht nach Westen gebogen, SW-NE verlaufende, ca. 80° nach NW einfallende Abschiebung als nordwestliche Grenze der Flintsbacher Jurakalk-Bucht in den Kristallingesteinen am Rand der Böhmischen Masse und versetzt den Paläo-Donaurandbruch [DE-BY_1237]. Geht im Süden in den Aidenbach-Griesbach Abbruch [DE-BY_764] über und begrenzt eine Scholle mit Jurakalk in geringer Tiefe (Fortsetzung der Flintsbacher Bucht) nach Nordwesten hin.
Flintsbach-Pleinting Fault
Eastward arcuate N-S trending, approx. 80° W dipping normal fault forming a moderate-throw pre-step of Aidenbach-Griesbach Step Fault [DE-BY_764]. Continues in Brand-Doblwiese Fault [DE-BY_1239] in the north and represents the eastern boundary of a downthrow block featuring Jurassic carbonates at shallow depth (continuation of Flintsbach embayment).
Flintsbach-Pleinting Störung
Ostwärts gebogen N-S verlaufende, rund 80° nach W einfallende Abschiebung, Vorbruch mäßiger Sprunghöhe zum Aidenbach-Griesbach Abbruch [DE-BY_764]. Nimmt im Norden die Brand-Doblwiese Störung [DE-BY_1239] auf und begrenzt eine Scholle mit Jurakalk in geringer Tiefe (Fortsetzung der Flintsbacher Bucht) nach Osten hin.
Ried Fault
Rieder Abbruch
Ried Störung
This undulate N-S trending, approx. 80° W dipping multiphase normal fault featuring a throw of up to 600 m runs in the subsurface of the Alpine Molasse from Bad Füssing (DE) via Ried im Innkreis (AT) towards the Attersee (AT). It is the southern continuation of Pocking Step Fault [DE-BY_699] on Austrian territory and is part of the Deggendorf-Ried Fault System [DE-BY_929, AT_1044]. It is confirmed by seismic and borehole data (Freudenberger & Schwerd 1996, Kröll et al. 2006). Its damage zone in the hanging wall is targeted by Ried-Mehrnbach geothermal development.
Diese gewellt N-S verlaufende, ca. 80° nach W einfallende mehrphasige Abschiebung mit einen Vertikalversatz von bis zu 600 m, im Molasseuntergrund von Bad Füssing (DE) über Ried im Innkreis (AT) bis zum Attersee verlaufende Störung ist durch Seismik- und Bohrlochdaten belegt (Freudenberger & Schwerd 1996, Kröll et al. 2006). Sie bildet die südliche Fortsetzung des Pockinger Abbruchs [DE-BY_699] und ist Teil der Deggendorf-Ried Störungssystems [DE-BY_929, AT_1044]. Die störungsbegleitende Zerrüttungszone der Tiefscholle ist der Zielbereich der geothermalen Erschließung Ried-Mehrnbach.
Birnbach-Füssing Step Fault
Weihmörting Fault Scarp
Weihmörtinger Abbruch
Birnbach-Füssing Abbruch
Southwestern branch of southern continuation of the Aidenbach-Griesbach Step Fault. Blind, undulate NNW-SSE trending, approx. 80° WSW dipping normal fault, featuring a cumulative throw of up to 1 km.
Südwestlicher Zweig der südlichen Fortsetzung des Aidenbach-Griesbach Abbruchs. Gewellt NNW-SSO verlaufende, ca. 80° nach WSW einfallende, überdeckte Abschiebung mit einer kumulativen Sprunghöhe bis zu 1 km.
Überdeckte E-W streichende, steil nach N einfallende Störung an der Basis des Molassebeckens die sich im Osten bis zur Ried Störung [AT-10654] als Teil des Deggendorf-Ried Störungssystems [DE-BY_929], im Westen bis Ranshofen (AT) zieht.
This E-W striking, steeply N-dipping blind fault at the bottom of the Molasse Basin terminates in the east at the Ried Fault [AT-10654], a branch of the Deggendorf-Ried Fault System [DE-BY_929], and in the west at Ranshofen (AT).
Nonsbach Fault
Nonsbach-Störung
Pfarrkirchen Fault
Pfarrkirchen Störung
NW-SE to NNW-SSE trending, approx. 70° ± NE dipping normal fault with a throw up to 800 m, running from Oberschneiding to Pfarrkirchen as an antithetic conjugated fault to Aidenbach-Griesbach Step Fault [DE-BY_764], and on to Simbach/Inn at the Austrian Border (kinematics uncertain) .
NW-SE bis NNW-SSE streichende, ca. 70° nach ± NE einfallende Abschiebung mit einem Versatz bis zu 800 m. Bildet von Oberschneiding bis Pfarrkirchen eine antithetische, konjugierte Störung zum Aidenbach-Griesbach Abbruch [DE-BY_764], die Fortsetzung bis zum Inn bei Simbach ist kinematisch unsicher.
Altenbuch-Oberpöring Subfault
Altenbuch-Oberpöring Nebenstörung
NNW-SSE striking, approx. 75° ENE dipping antithetic normal fault southwest of Plattling; branch of Pfarrkirchen Fault [DE-BY_ 763].
NNW-SSE streichende, ca. 75° nach ENE einfallende antithetische Abschiebung südwestlich von Plattling; Zweig der Pfarrkirchen Störung [DE-BY_ 763].
Überdeckte, ENE-WSW streichende, N-fallende Störung an der Basis des Molassebeckens, die sich vom Landshut-Neuötting Abbruch im Westen über Mattighofen (AT) bis zur Ried Störung [AT-10654] zieht. Diese Störung ist in der Bohrung Steindlberg 1 nachgewiesen.
Steindlberg Fault
Steindlberg-Störung
This ENE-WSW striking, N-dipping blind fault at the bottom of the Molasse Basin runs via the town of Mattighofen (AT) terminates in the west at the Landshut-Neuötting Fault System and in the east at the Deggendorf-Ried Fault. The Fault is observed at Well Steindlberg 1.
This SE-NW striking, NE-dipping blind fault at the bottom of the Molasse Basin starts east of Braunau (AT) and runs via Mauerkirchen (AT) towards SE and terminates at the Handenberg Fault [AT-10655].
Überdeckte, SE-NW streichende, NE-fallende Störung an der Basis des Molassebeckens, die sich von Braunau (AT) im Westen über Mauerkirchen (AT) bis zur Handenberg Sörung [AT-10655] zieht.
Mauerkirchen Fault
Mauerkirchen-Störung
Karlstift Fault System
The Karlstift fault system consists of several parallel NNE-SSW trending faults from Nove Hrady (CZ) at the northern end via Höhenberg (AT) towards Lasber or Erdleiten at the southern end. In analogy to the Rodl fault system, the main ductile deformation phase is dated to the Late Variscian, showing mainly right-lateral movement. Late Miocene reactivation, again with right-lateral movement, is assumed. (Brandmayr et al., 1997; Büttner, 2007)
Das Störungssystem besteht aus mehreren parallel, NNE-SSW streichenden Störungen, die sich von Nove Hrady (CZ) und Höhenberg (AT) nach Süden bis Lasber bzw. Erdleiten verfolgen lassen. Die duktile Hauptbewegungsphase wird, analog zum Rodl-Störungssystem, auf das Spätvariszikum gelegt, mit hauptsächlich sinistraler Bewegungsrichtung. Von einer spröden miozänen Reaktivierung mit derselben Bewegungskinematik wird ebenfalls ausgegangen. (Brandmayr, 1997; Büttner, 2007)
Karlstift-Störungssystem
The approximately SW-NE striking fault runs from Prätis to east of Vorau.
Vorau Fault
Vorau-Störung
Die in etwa SW-NE-streichende Störung verläuft von Prätis bis östlich von Vorau.
Kalkstein-Vallarga Fault System
This ca. 50 km long, approximately NNE-SSW trending Fault System south of the Tauern window extends from the Weiten (Vallarga) Valley to Kalkstein (southwest of Innervillgraten). In analogy to the Defereggen-Antholz-Vals Fault System, it shows ductile movement during Cretaceous and Paleogene times with brittle left-lateral movement during Oligocene and early Miocene times (Handy et al., 2005).
Ist ein in etwa WNW-ESE-streichendes ca. 50 km langes Störungssystem südlich des Tauern-Fensters, welches von Weitental (Vallarga) bis Kalkstein (südwestlich von Innervillgraten) reicht. Vergleichbar zum Defreggen-Antholz-Vals-Störungssystem wird eine duktile Anlage in der Oberkreide-Paläogen angenommen mit einer deutlichen sinistral seitenverschiebenden spröden Überprägung im Oligozän bis unterstem Miozän (Handy et al., 2005).
Kalkstein-Vallarga-Störungssystem
The E-W striking fault runs from 4 km south of Fieberbrunn via Leogang to Bachwinkl Pabing.
Die E-W striking Störung verläuft vom 4 km südlich von Fieberbrunn über Leogang nach Bachwinkl Pabing.
Leogang Fault
Leogang-Störung
Mölltal Fault System
This ca. 65 km long, NE-SW trending Fault System extends from Obervellach, following the Möll Valley to Villach and the Drau Valley, where it is cut by the Periadriatic Fault System. It shows ductile and brittle right-lateral movement with a main activity during Miocene times. An initiation in the Oligocene and continuation to the Tauern window is discussed (Scharf et al., 2013 and references therein). Displacement rates from 20 to 45 km are described (Linzer et al, 2002).
Dieses NW-SE-streichende ca. 65 km lange Störungssystem verläuft von Obervellach, entlang des Mölltals über Villach bis zum Drautal. Dort geht es ins Periadriatisches-Störungssystem über bzw. wird von diesem abgeschnitten. Es zeigt duktile, vorwiegend dextral seitenverschiebende Kinematik mit einer Hauptaktivität im Miozän. Eine Anlage im Oligozän mit Übergängen ins Tauern-Fenster wird diskutiert (Scharf et al., 2013 und die darin aufgeführten Referenzen) und ein Versatz von 20-45 km wird angenommen (Linzer et al, 2002).
Mölltal-Störungssystem
Jachymov Fault System
The NW-SE trending Fault System extends from Strakonice (CZ) via České Budějovice and Trebon to Gmünd (AT). The associated faults show evidences for dextral and normal movement between the late Variscan and Miocene. (Brandmayr et al., 1997; Porparczy, 2011)
Das NW-SE streichende Störungssystem, auch unter dem Namen Joachimsthal-Störungssystem bekannt, zieht sich von Strakonice (CZ) über die Budweis- und Trebon-Becken bis nach Gmünd (AT) hin. Die Störungen zeigen Hinweise sowohl auf dextrale wie auch abschiebende Deformation zwischen dem späten Variszikum und post-Miozän. (Brandmayr et al., 1997; Porparczy, 2011)
Jachymov-Störungssystem
This NW-SE striking fault is the SE-bounding fault of the České Budějovice (Budweis) basin and runs from Dehtare to Borsov nad Vlatavou (CZ).
Diese NW-SE-streichende Störung ist die SE-Begrenzung des Budweiser Beckens und verläuft von Dehtare nach Borsov nad Vlatavou (CZ).
Dubno Fault
Dubno-Störung
This slightly curved, NNE-SSW trending fault runs from Mittersill via the summit of M. Schrankeck to east of M. Stollkogel in the south.
Diese leicht gebogene, NNE-SSW-streichende Störung verläuft von Mittersill über die Erhebung des Schrankecks bis östlich des Stollkogels im Süden.
Stollkogel-Schrankeck Fault
Stollkogel-Schrankeck-Störung
Kourim-Blanice-Rodl-Kaplice Large-scale Fault System
This ca. 250 km long, approximately NNE-SSW (and partly NNE-SSW) trending large-scale fault system extends from the Kourim Furrow in the North, following the Blanice Furrow, crossing the basins of Trebon and České Budějovice via Kaplice (CZ) and the valley of the Große Rodl to Gramastetten and the basin of Eferding, where it is partly covered by Miocene sediments, but continues into the basin subsurface (Brandmayr et al., 1997, Wagner, 1998, Zacharias & Hübst, 2012). It includes the Kourim-Blanice and Rodl-Kaplice Fault Systems and shows a long-lasting and multiphase deformation history. Parallel trending structures and conjugated shear zones and faults are correlated with this large-scale fault system (e.g. Haselgraben Subfault System). Proofs of NE-SW-trending left-lateral strike-slip ductile, mylonitic shear zones during Upper Carboniferous and Permian times are predominantly observed in the southern parts (Brandmayr, et al., 1995; Büttner, 2007, Iglseder, 2013). To the North, it continues to build horst-and-graben structures filled with Upper Carboniferous to Permian sediments (Martinek et al., 2001) and associated Permian dykes (Kosler et al., 2001). The deformation continued as left-lateral strike-slip faulting during Cretaceous and Miocene times, indicated by sediment deposits (Iglseder, 2013).
Dieses in etwa NNE-SSW - (teilweise NNE-SSW-) streichende ca. 250 km lange Großstörungssystem zieht vom Kourim-Becken, entlang dem Blanice-Graben, dem Becken von Trebon und dem Becken von Budweis über Kaplice, das Große Rodl-Tal entlang bis Gramastetten und wird im Eferding-Becken von Miozänen Sedimenten überdeckt, setzt sich jedoch in den kristallinen Beckenuntergrund fort (Brandmayr et al., 1997, Wagner, 1998, Zacharias & Hübst, 2012). Es setzt sich aus dem Kourim-Blanice- und Rodl-Kaplice-Störungssystem zusammen und zeigt eine langandauernde und multiphase Entwicklung. Parallel streichende Strukturen und konjugierte Scherzonen und Störungen orientiert als Riedel und Antiriedel werden diesem Großstörungssystem zugeordnet (z.B. Haselgraben-Teilstörungssystem). Die Anlage als NE-SW-streichende duktile mylonitische Scherzonen mit sinistral seitenverschiebender Kinematik des oberen Karbons bis Perms (Brandmayr, et al., 1995; Büttner, 2007) sind vorwiegend in den südlichen Abschnitten beschrieben und setzt sich nach Norden in von oberkarbonen-permischen Sedimenten verfüllte (Martinek et al., 2001) mit permischen Gängen assoziierte Horst und Grabenstruktur fort (Kosler et al., 2001). Diese wird durch spröde Störungen mit sinistral seitenverschiebender Kinematik überprägt (Iglseder, 2013), welche sich anhand von Beckenfüllungen über die Oberkreide bis ins Miozän beobachten lassen.
Kourim-Blanice-Kaplice-Rodl-Großstörungssystem
Rodl-Kaplice Fault System
This ca. 90 km long, approximately NNE-SSW trending fault system extends from Kaplice (CZ), following the valley of the Große Rodl to Gramastetten and the basin of Eferding, where it is partly covered by Miocene sediments, but continues into the basin subsurface (Brandmayr et al., 1997, Wagner, 1998). It includes the Rodl and Haselgraben Subfault Systems and shows a long-lasting and multiphase history. Proofs of NE-SW-trending left-lateral strike-slip ductile mylonitic shear zones during Upper Carboniferous and Permian times are observed (Brandmayr, et al., 1995; Büttner, 2007, Iglseder, 2013). The deformation continuous with left-lateral strike-slip faulting during Cretaceous and Miocene times, indicated by sediment deposits (Iglseder, 2013). Displacement up to 35 km is suggested (Iglseder, 2013).
Dieses etwa NNE-SSW - streichende ca. 90 km lange Störungssystem zieht von Kaplice, das Große Rodl-Tal entlang bis Gramastetten und wird im Eferding-Becken von Miozänen Sedimenten überdeckt, setzt sich jedoch in den kristallinen Beckenuntergrund fort (Brandmayr et al., 1997, Wagner, 1998). Es beinhaltet das Rodl- und Haselgraben-Teilstörungssystem sowie parallel orientierte und konjugierte Strukturen. Eine erste Prägung erfuhren diese NE-SW-streichenden duktilen mylonitischen Scherzonen mit sinistral seitenverschiebender Kinematik im oberen Karbon – Perm (Brandmayr et al., 1995, Büttner, 2007). Diese wird durch spröde Störungen mit sinistral seitenverschiebender Kinematik überprägt (Iglseder, 2013), welche sich anhand von Beckenfüllungen über die Oberkreide bis ins Miozän, sowie Versatz von Miozänen Sedimenten verfolgen lässt. Sinistrale Versatzweiten von bis 35 km werden angenommen (Iglseder, 2013).
Rodl-Kaplice-Störungssystem
Haselgraben Subfault System
This ca. 15 km long N-S trending subfault system extends from Hellmondsödt, following the Haselgraben Valley to Linz. It is part of the Rodl-Kaplice Fault System and includes ductile parallel trending shear zones with left-lateral kinematics active during the Late Variscian. In analogy to the Rodl Subfault System, a continuation of brittle left-lateral movement during Cretaceous and Miocene times is suggested. (Iglseder, 2013, 2014a, b)
Dieses ca. 15 km lange N-S-streichende Teilstörungssystem verläuft von Hellmondsödt, den Haselgraben entlang bis Linz und ist Teil des Rodl-Kaplice-Störungssystems. Es beinhaltet duktile parallel verlaufende Scherzonen mit sinistral seitenverschiebender Kinematik aktiv während des Spätvariszikums. Analog zum Rodl-Teilstörungssystem wird eine spröde Reaktivierung mit sinistral-seitenverschiebender Bewegung während der Kreide bis Miozän angenommen. (Iglseder, 2013, 2014a, b)
Haselgraben-Teilstörungssystem
The N-S trending fault is part of Haselgraben Subfault System and extends from Hellmannsödt in the north along the Haselgraben Valley via Linz to the south of Hofkirchen im Traunkreis (Iglseder, 2013, 2014a, b).
Die N-S streichende Störung ist Teil des Haselgraben-Teilstörungssystems. Sie erstreckt sich von Hellmannsödt im Norden entlang des Haselgrabens via Linz bis nach Hofkirchen im Traunkreis im Süden (Iglseder, 2013, 2014a, b).
Haselgraben Fault
Haselgraben-Störung
This ca. 55 km long, approximately NNE-SSW trending Subfault System extends from Rybnik (CZE), following the Valley of the Große Rodl to Gramastetten and the basin of Eferding, where it is partly covered by Miocene sediments, but continues in the basin subsurface (Brandmayr et al., 1997, Wagner, 1998). It includes partly parallel trending shear zones and faults and shows a long-lasting and multiphase history. Proofs of NE-SW-trending left-lateral strike-slip ductile, mylonitic shear zones during upper Carboniferous and Permian times are observed (Brandmayr, et al., 1995; Büttner, 2007, Iglseder, 2013). The deformation continuous with left-lateral strike-slip faulting during Cretaceous and Miocene times, indicated by sediment deposits. Displacement up to 35 km is suggested. (Iglseder, 2013)
Rodl Subfault System
Dieses NNE-SSW - streichende ca. 55 km lange Teilstörungssystem zieht von Kaplice, das Große Rodl-Tal entlang bis Gramastetten und wird im Eferding-Becken von Miozänen Sedimenten überdeckt, setzt sich jedoch in den kristallinen Beckenuntergrund fort (Brandmayr et al., 1997, Wagner, 1998). Eine erste Prägung erfuhren diese NE-SW-streichenden duktilen mylonitischen Scherzonen mit sinistral seitenverschiebender Kinematik im oberen Karbon – Perm (Brandmayr et al., 1995, Büttner, 2007). Diese wird durch spröde Störungen mit sinistral seitenverschiebender Kinematik überprägt (Iglseder, 2013), welche sich anhand von Beckenfüllungen über die Oberkreide bis ins Miozän, sowie durch den Versatz von Miozänen Sedimenten verfolgen lässt. Sinistrale Versatzweiten von bis 35 km werden angenommen. (Iglseder, 2013)
Rodl-Teilstörungssystem
The mylonitic part of the NNE-SSW trending Rodl Subfault System is referred to as Rodl Shearzone.
Die in etwa NNE-SSW-streichende Scherzone umfasst den duktilen Teil des Rodl-Teilstörungssystem.
Rodl Shearzone
Rodl-Scherzone
The approximately NNE-SSW trending fault contains the brittle part of the Rodl Subfault System.
Die in etwa NNE-SSW-streichende Störung umfasst den spröden Teil des Rodl-Teilstörungssystems.
Rodl-Störung
Rodl Fault
Vils Fault
The NW-SE striking fault runs from Steinach (Ger) via Vils and Reutte to the lake Plansee. The map view suggests left-lateral offset. (Tollmann, 1986)
Die NW-SE streichende Störung verläuft von Steinach (D) über Vils und Reutte zum Plansee. Aus dem Kartenbild ergibt sich ein sinistraler Versatz. (Tollmann, 1986)
Vils-Störung
NCA NNE-SSW Fault Set
This fault set of NNE-SSW trending faults within the Northern Calcareous Alps (NCA) includes the Göstling Fault, the Leonsberg Fault, the Untersalzachtal Fault, the Weyer Fault and other similar orientated faults with same kinematics. Even though they may have been active during Oligocene and Miocene times as sinistral or dextral strike-slip faults, respectively, the main deformation phase of this conjugated fault set occurred during Middle Miocene E-W extension, where the faults had normal fault kinematics. (Peresson & Decker, 1997a, b)
Dieses Störungsset beinhaltet NNE-SSW-streichenden Störungen in den Nördlichen Kalkalpen (NKA), welche die Göstling-, Leonsberg-, Untersalzachtal-, Weyer- und weitere ähnlich orientierte Störungen mir derselben Kinematik beinhaltet. Diese Störungen waren während des Oligozäns-Miozäns als sinistrale und dextrale Seitenverschiebungen aktiv. In ihrer Hauptphase während des mittleren Miozäns zeigen sie abschiebende Kinematik. (Peresson & Decker, 1997a, b)
NKA-Störungsset (NNE-SSW)
The NNW-SSE trending fault with left-lateral movement runs along valley of the River Salzach between Golling/Salzach and Salzburg. (Frisch & Gawlick, 2003)
Die NNW-SSE-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft im Bereich des unteren Salzachtales etwa zwischen Golling a.d. Salzach bis Salzburg. (Frisch & Gawlick, 2003)
Untersalzachtal Fault
Untersalzachtal-Störung
The NNE-SSW trending fault with left-lateral movement runs from Hieflau through Göstling to 3 km west of Ybbsbachamt. (Decker et al., 1993, 1994; Linzer et al., 2002)
Die NNE-SSW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft von Hieflau über Göstling bis 3 km westlich von Ybbsbachamt. (Decker et al., 1993, 1994; Linzer et al., 2002)
Göstling Fault
Göstling-Störung
The NNE-SSW trending fault runs east of the lake Attersee. (Tollmann, 1986)
Die NNE-SSW-streichende Störung verläuft östlich des Attersees. (Tollmann, 1986)
Leonsberg Fault
Leonsberg-Störung
The NNE-SSW trending fault with left-lateral movement runs from Admont to Neudorf, north of Weyer. (Decker, et al., 1994; Linzer et al., 2002)
Die NNE-SSW-streichende Störung mit sinistral seitenverschiebender Kinematik verläuft von Admont nach Neudorf, nörlich von Weyer. (Decker, et al., 1994; Linzer et al., 2002)
Weyer Fault
Weyer-Störung
The approximately NW-SE trending fault runs from 3 km SW of St. Nikolai/Sölktal to Baierdorf.
Die etwa NW-SE-streichende Störung verläuft von 3km südwestlich von St. Nikolai im Sölktal bis Baierdorf.
Katschbachtal Fault
Katschbachtal-Störung
The E-W striking normal fault runs from Scheidersdorf to Sitzendorf. Top to the south faulting was active during the Eggenburgium.
Die E-W-streichende Abschiebung verläuft von Scheidersdorf bis Sitzendorf, die Bewegungsrichtung des Hangendblocks ging im Eggenburgium gegen Süden.
Mödring Fault
Mödring-Störung
Moldanubian Thrust
Along this Variscian E-dipping shear zone, the Moldanubian Superunit moves NNE-vergent over the Moravo-Silesian Superunit. The fault strikes N-S from Langenlois to Horn, where it extends in WNW-ESE direction towards Messern. There, the fault strikes NE-SW via Geras and Vranov (CZ) to Moravský Krumlov (CZ). (Fritz & Neubauer, 1994; Stipska et al., 1999)
Jungvariszische E-einfallende Scherzone, an der das Moldanubikum NNE-vergent über das Moravikum geschoben wurde. Sie verläuft N-S streichend von Langenlois bis östlich von Horn, wo sie dann WNW-ESE streichend bis Messern verläuft. Dort ändert sie wiederum ihre Streichrichtung und verläuft NE-SW streichend über Geras und Vranov (CZ) bis nach Moravský Krumlov (CZ). (Fritz & Neubauer, 1994; Stipska et al., 1999)
Moldanubische Scherzone
Mattersburg Fault
The Mattersburg fault consists of two NW-SE striking and steeply NE-dipping subfaults that extend from Wiener Neustadt via Mattersburg to the Austrian-Hungarian border. Based on the Molasse subsurface map, it has a normal fault character with an offset of up to 1000 m. (Wessely et al., 1993)
Die Mattersburg-Störung besteht aus zwei NW-SE streichenden, steil nach NE einfallenden Teilstörungen, die sich von Wiener Neustadt über Mattersburg bis zur ungarischen Grenze hinziehen. Aus der Molasseuntergrundkarte ist ein abschiebender Charakter mit Versatzweiten bis zu 1000 m ablesbar. (Wessely et al., 1993)
Mattersburg-Störung
Hochstuhl-Gegendtal Fault System
This ca. 55 km long, approximately NNW-SSE trending Fault System extends from the Hochstuhl mountain (at the AUT-SLO border), following the Gegendtal (Afritz) Valley to Radenthein. Proofs for right-lateral movement from the Miocene with thrusting along the Rosegg shear zone with displacement rates up to 20 km as well as displacement of the Periadriatic Fault System of 3,5 km are described. (Polinski & Eisbacher, 1992)
Dieses in etwa NNW-SSE - streichende ca. 55 km lange Störungssystem zieht vom Hochstuhl (an der AUT-SLO Grenze), bis Rosegg und weiter über das Gegendtal (Afritzbach) nach Radenthein. Es zeigt dextral seitenverschiebende Kinematik ab dem Miozän mit überschiebender Kinematik entlang der Rosegg-Scherzone. Versatzweiten von bis zu 20 km mit einem Versatz des Periadriatischen Störungssystem von 3,5 km ist beschrieben. (Polinski & Eisbacher, 1992)
Hochstuhl-Gegendtal-Störungssystem
The NW-SE trending fault in the area of the Hochstuhl Mountain from north of Millstatt to Zauchen shows right-lateral displacement and is part of the Hochstuhl-Gegendtal Fault System (Polinski & Eisbacher, 1992).
Die NW-SE-streichende Störung des Hochstuhl-Gegendtal-Störungssystem von Millstatt nach Zauchen zeigt dextral-seitenverschiebende Kinematik (Polinski & Eisbacher, 1992).
Hochstuhl Fault
Hochstuhl-Störung
Pregarten Fault
The NW-SE striking fault runs from Pregarten via Kriechbaum to Oberlebing. It forms the NE margin of the Gallneukirchen Basin. (Kröll et al., 2001; Seiberl et al., 1996)
Die NW-SE streichende Störung verläuft von Pregarten über Kriechbaum nach Oberlebing. Sie formt die NE-Grenze des Gallneukirchen-Beckens. (Kröll et al., 2001; Seiberl, et al., 1996)
Pregarten-Störung
Pöll Fault
The WSW-ENE striking fault runs from the Ochsenkogel mountain south of Leoben via the Hochalpe mountain and the village of Kirchdorf to Stanz im Mürztal. (Tollmann, 1986)
Die WSW-ENE streichende Störung verläuft vom Ochsenkogel südlich von Leoben über die Hochalpe und Kirchdorf nach Stanz in Mürztal. (Tollmann, 1986)
Pöll-Störung
This is a ca. 70 km long, roughly WE-trending fault system (FS) south of the Tauern window, which runs from Vals (north of Brixen) via the Valleys of Antholz and Defereggen to Huben in the Valley of the Isel, where it is cut by the Iseltal Fault. Proofs of pre-existing nappe boundaries, ductile, mylonitic shear zones with low angle normal faulting and top E sense of shear and partly left-lateral transpressive kinematics during Cretaceous and Paleogene times are observed. Followed by dextral strike-slip transtensive kinematics (parallel to the Rieserferner plutonic body) from the upper Oligocene to the Miocene. (Mancktelow et al., 2001)
Das etwa W-E-streichende ca. 70 km lange Störungssystem südlich des Tauern-Fensters verläuft von Vals (nördlich von Brixen) über das Antholz- und Defereggental bis Huben im Iseltal, wo es von der Iseltal-Störung abgeschnitten wird. Eine kreidezeitliche bis Paläogene Anlage mit duktilen Myloniten in niedrigwinkelig abschiebenden Scherzonen mit top E-gerichteten Schersinnen und sinistral transpressiver Kinematik bis ins obere Oligozän (parallel zur Intrusion des Rieserferners) ist beschrieben. Diese wurde von dextral transtensiver Kinematik im Miozän überprägt. (Mancktelow et al., 2001)
Defereggen-Antholz-Vals Fault System
Defereggen-Antholz-Vals-Störungssystem
Tauern Window Subfault System
This ENE-WSW, partly NE-SW trending Subfault System is a fault set of parallel and conjugated shear zones and faults in the western part of the Tauern window with ductile left-lateral movement during the Miocene (Schneider et al., 2013). It includes the Ahorn-, Olperer-, Tux-, Greiner-, and Ahrntal Shear zones amongst other similar orientated faults with same kinematics.
Dieses ENE-WSW-, teilweise NE-SW-streichende Teilstörungssystem ist ein Störungsset von parallel verlaufenden und konjugierten Scherzonen und Störungen im westlichen Tauernfenster mit duktiler, sinistral seitenverschiebender Kinematik aktiv während des Miozän (Schneider et al., 2013). Es beinhaltet die Ahorn-, Olperer-, Tux-, Greiner- und Ahrntal-Scherzonen sowie weitere ähnlich orientierte Scherzonen und Störungen.
Tauernfenster-Teilstörungssystem
The ENE-WSW trending ductile shear zone in the western Tauern window with left-lateral movement was active during the Miocene. (Hintersberger & Iglseder, 2017 subm.)
Die ENE-WSW-streichende Scherzone im westlichen Tauernfenster mit duktiler, sinistral seitenverschiebender Kinematik war während des Miozäns aktiv. (Hintersberger & Iglseder, 2017)
Unlasseck-Leiterer Shear Zone
Unlasseck-Leitherer-Scherzone
The ENE-WSW trending ductile shear zone in the western Tauern window with left-lateral movement was active during the Miocene. (Schneider et al., 2013)
Die ENE-WSW-streichende Scherzone im westlichen Tauernfenster mit duktiler, sinistral seitenverschiebender Kinematik war während des Miozäns aktiv. (Schneider et al., 2013)
Greiner Shear Zone
Greiner-Scherzone
The ENE-WSW trending ductile shear zone in the western Tauern window with left-lateral kinematics was active during the Miocene. (Schneider et al., 2013)
Ahrntal Shear Zone
Ahrntal-Scherzone
Gurktal Alps Subfault System
This WNW-ESE and partly NW-SE trending Subfault System consists of parallel trending conjugated faults in the Gurktal Alps, showing top-to-the-WNW thrusting and right-lateral strike-slip faults since late Eocene times. (Ratschbacher et al., 1989)
Dieses WNW-ESE-, teilweise NW-SE-streichende Teilstörungssystem ist ein Störungsset von parallel verlaufenden und konjugierten Störungen in den Gurktaler Alpen, welche post-Eozäne top WNW-aufschiebende und dextral seitenverschiebende Kinematik zeigen. (Ratschbacher et al., 1989)
Gurktaler Alpen-Teilstörungssystem
Gurk Fault
This NW-SE trending fault is part of the Gurktal Alps Subfault System. (Oberhauser & Bauer, 1980)
Ist eine NW-SE-streichende Störung des Gurktaler-Alpen-Teilstörungssystems. (Oberhauser & Bauer, 1980)
Gurk-Störung
Trogscharten Fault
The steep NW-SE striking fault runs from St. Lorenzen ob Murau to Grades im Meinitz Tal. Presumably, the eastern block was lowered. (Neubauer, 1980)
Die steilstehende NW-SE streichende Störung verläuft von St. Lorenzen ob Murau bis Grades im Meinitz-Tal. Vermutlich wurde der Ostblock abgesenkt. (Neubauer, 1980)
Trogscharten-Störung
The approximately E-W striking right lateral brittle strike-slip fault runs from Nenzing to Roppen (Buchroithner, 1984; Tollmann, 1986).
Klostertal Fault
Klostertal-Störung
Tectonic Boundary in Germany
The fault data considered are characterized by regional variations in density and detail, different degree of generalization and origin. Therefore, different display scales are recommended for the respective data sets: 1.) German onshore (1: 2500000 - 1: 500000), 2.) Baltic Sea (1:1000000 - 1:250000), 3.) Central German North Sea (1:1000000 - 1:100000), 4.) Entenschnabel region - The northwestern German North Sea sector (1:1000000 - 1:50000). The focus of the concepts presented here follows the idea of assigning faults to different structural (sub)domains, each characterized by a specific tectonic-sedimentary development. The fault data of the Central German North Sea consist of generalized fault intersections with 13 Mesozoic to Cenozoic horizons and the Late Paleozoic Base Zechstein (Baldschuhn et al. 2001). For the northwestern part of the German North Sea, the Entenschabel, faults originate on interpretations of 3D-seismic data from the GPDN-Project (https://www.gpdn.de/; Arfai et al. 2014). Fault data of the Baltic Sea are based on the studies of Seidel et al. (2018), Seidel (2019) and fault intersections of 13 Mesozoic to Cenozoic horizons as well as the base Zechstein and base Upper Rotliegend from Doornenbal & Stevenson (2010). For the HIKE-fault data base these fault intersections were assigned, where useful, to individual faults or fault systems. Even if fault intersections spatially overlap, a direct linkage of a Meso-Cenozoic fault with the Pre-Zechstein must be questioned, as salt often acts as a decoupling element between the overburden and basement. Fault data for the onshore area of Germany originate on the data compiled within the Geothermal Atlas (Schulz et al. 2013). These data are made up of an integration and merging from different map series, such as e.g. the Geological surface map of Germany (e.g., Toloczyki et al., 2006), the Geotectonic Atlas of North West Germany and the German North Sea Sector (e.g., Baldschuhn et al. 2001), the Southern Permian Basin Atlas (e.g., Doornenbal & Stevenson 2010). The presented spatial data of faults consists exclusively of generalized, horizon independent lineaments from overview structure maps or of generalisations from surface maps. At this point it should be noted that the generalization accomplished in the frame of the Geothermal Atlas originally not includes a crosscheck of the geological state authorities. The necessary generalization and harmonization of faults in an overview scale may therefore differ in details from detailed data hosted by geological state authorities of Germany.
Representations of principal and overarching tectonic boundaries displayed in the HIKE Fault data base presented for entire Germany by the BGR are in an overview scale and are named by the notation DE. For some German Federal States, more detailed concepts are available with prefixed DE-ISO 3166-2 code.
Rhenish Massif domain
The SW-NE striking Rhenish Massif domain represents a long-living Mesozoic to Tertiary basement high. Most of the rocks show a Variscan age deformation. It is bordered to the south by the Hunsrück southern rim fault (DE-29) and Taunuskamm thrust (DE-189) and to the North by the Münsterland Cretaceous basin. [Domain type: Variscan basement block, Basement: Rhenohercynian.]
We describe the Rhenish Massif as a tectonostratigraphic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein. The extent of this structural unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Eifel North - South zone subdomain
Eifel North - South zone fault set
A North-South oriented zone in the transition from the Rhenish Schiefergebirge to the Ardennes. In the south the Triassic of the Trier Bight & Gulf of Luxembourg lies on the Rhenish Massif. The kinematics and history of this structural element have not yet been clarified. [Domain type: Undefined crustal zone, Basement: Rhenohercynian.]
We describe the Eifel North - South Zone as a diffuse tectonic element, a N-S striking syncline with relicts of Mesozoic strata on top. The unit is roughly defined by the extent of the syncline. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Bopparder thrust
Ebbe thrust
Ennepe fault
Oberhausener fault
Rauendahl fault
Rauendahler fault
Undefined fault within the Münsterland Cretaceous Basin
Sackpfeifen thrust
Siegen main thrust
Taunuskamm thrust
Wittlich Depression subdomain
Wittlicher depression fault set
Wittlicher depression
Permo-Carboniferous basin relict on top of Rhenohercynian basement. [Domain type: Post-Variscan basement block, Basement: Rhenohercynian.]
We describe the Wittlich depression as a tectonostratigraphic Permo-Carboniferous basement unit on top of Rhenohercynian basement whose boundaries are defined by faults and especially by lithological changes. The extent of this structural unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Neuwieder Basin subdomain
Neuwieder Basin
Tertiary to Quaternary Basin. [Domain type: Sedimentary overburden, Basement: Rhenohercynian.]
We describe the Neuwieder Basin as a Quaternary tectonostratigraphic unit on top of Rhenohercynian basement whose boundaries are defined by faults and especially by lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
German Cenozoic Volcanic regions
We describe the German Cenozoic Volcanic regions as a compilation of Cenozoic-Quaternary (rather rare Late Cretaceous) volcanic fields/regions, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outlines of each volcanic field/region was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Accompanied with the formation of the ECRIS an up to 1200 km wide intraplate magmatism developed, also known as European Cenozoic Volcanic province (ECVP). Only few centers of volcanism are located directly within the graben formed in the context of ECRIS. Instead, some are located up to 200 km away from the rift structures. In Germany the main centers are the Vogelsberg, Eifel, Westerwald and Rhön (Fig. 19a, country sheet).
Urach Volcanic field
We describe the Urach volcanic field as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Westerwald Volcanic field
We describe the Westerwald volcanic field as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Siebengebirge volcanic field
The Siebengebirge volcanic field subdomain belongs to the European Cenozoic Volcanic province and is located at the Rhenish Massif domain.
We describe the Siebengebirge volcanic field as a volcanic field whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Rhön Volcanic field
The Rhön Volcanic field subdomain belongs to the European Cenozoic Volcanic complex and is characterized by Saxonthuringian - Mid-German crystalline high basement.
We describe the Rhön volcanic field as a volcanic field whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
East Eifel volcanic field
The domain of the Eifel volcanic field belongs to the European Cenozoic Volcanic province and is characterized by Pleistocene to recent activity. Volcanic centers are aligned at SE-striking faults.
We describe the East Eifel volcanic field as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
West Eifel volcanic field
We describe the West Eifel volcanic field as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Vogelsberg volcanic complex
We describe the Vogelsberg volcanic complex as a volcanic complex whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Hegau Volcanic field
The Hegau Volcanic field subdomain belongs to the European Cenozoic Volcanic complex domain and is assumed to be associated with the Freidorf-Bonndorf fault system. Age outcrop: Middle Miocene (volcanics), Neogene (Molasse sediments)
We describe the Hegau as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Heldburg Gangschar
The Heldburg Gangschar subdomain belongs to the European Cenozoic Volcanic complex domain and is characterized by NNE to N striking volcanic dykes of Eocene to Middle Miocene age.
We describe the Heldburg Gangschar as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Hocheifel Volcanic field
The Hocheifel volcanic field subdomain belongs to the European Cenozoic Volcanic complex domain and the Eifel plume therein.
We describe the Hocheifel volcanic field as a volcanic field, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic field was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
Lausitz Volcanic complex
The Lausitz volcanic complex subdomain belongs to the European Cenozoic Volcanic complex domain and is located SE of the Lausitz Block domain.
We describe the Lausitz volcanic complex as a volcanic complex whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic complex was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
North Hessian volcanic complex
The North Hessian Volcanic complex subdomain belongs to the European Cenozoic Volcanic complex, is located within the Hessian depression and characterized by Rhenoherzynian basement.
We describe the North Hessian volcanic complex as a volcanic complex, whose boundaries are defined by the todays distribution of effusive rocks and volcanos. The here used outline is only a rough estimate of the volcanic region with regard to a further necessary inclusion of additional indications for volcanic activity (e.g. mofettes, seismicity - earthquake swarm regions, uplift). The outline of the volcanic complex was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
North German Basin - domain II: uplifted and/ or inverted southern regions of the North German Basin
We define here the North German Basin - domain II as a tectonostratigraphic unit, whose boundaries are defined both by faults and fault systems, often fuzzy trends in the lithofacies and, in particular by the expression of deformation events. The division into two domains of the North German Basin (NGB) is intended to indicate in particular the uplift of some basin regions during the Late Cretaceous and the associated different levels of erosion in this region. Depending on the level of erosion and the preservation of signs of former deformation phases, this results in regionally partly different dominant fault patterns, even if these deformation phases have influenced almost the entire basin. The Lower Saxony Basin, which was actually also strongly inverted during the Late Cretaceous, should therefore actually be part of domain II of the NGB: uplifted and/ or inverted southern regions of the North German Basin. However, it is also largely part of the German lowlands. In this respect, the subdivision made here should only be understood as a rough classification. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
This tectonic domain covers uplifted areas of some regions of the southern NGB. Structures within the southern NGB were partly inverted or steep basement thrusts were created during the Late Cretaceous. The result is a much stronger erosion of the Mesozoic basin fill as in the northern parts of the NGB.
southern Eichsfeld-Altmark Swell
We define here the Eichsfeld-Altmark Swell as a tectonostratigraphic sub-domain of the North German Basin, whose boundaries are not clearly defined by faults and fault systems. The outline of the domain can only be roughly defined based on lithostratigraphic trends and on the base of differences in the deformation pattern to surrounding areas. But several NNE-striking fault zones and grabens lies within this tectonic unit. Even though the main structures of this region have been described in detail (e. g. Röhling, 1991, Baldschuhn et al., 2001), no clear definition of the outline of this feature has been made to date. Even if the swell still includes large regions in the eastern LSB (DE-917) and along the area of the Braunschweig-Gifhorn-Lüneburg fault system (DE-937), only faults in the east of the Hessian Depression (southern segment of the swell) in particular are assigned to this domain in this classification. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
The Eichsfeld-Altmark Swell represents a supra-regional, long living swell, which has impact on the tectono-sedimentary development of several structural regions within the NGB, such as parts of the Thuringian Depression, the Braunschweig-Gifhorn-Lüneburg fault system, Altmark-Fläming Depression, Lower Saxony Basin or the Leinetal Graben and also on parts of the southwestern fringe of the Bohemian Massif subdomain. Domain type: Supra-regional long-living swell, Main-Activity: Permian, Triassic, important separating element during Late Cretaceous contraction; Basement: mainly Rhenohercynian, within the inner part also Northern Phyllite Zone and within the outer part also Avalonia & Saxothuringian.
Leinetal graben fault system
Harz western boundary fault
The Harz western boundary fault extends over 52 km in N-S direction along the western rim of the Harz.
Oberkatz graben fault system
Werra Uplift
The Werra Uplift is a ESE/SE striking Late Cretaceous basement high/anticline SW of the Harz between the Hessian Depression in the west and the Thuringian Syncline in the east. Paleozoic sediments are exposed in the core area of the uplift. However, the majority of this uplift structure is covered by Triassic sediments.
faults in the Rhenohercynian units of the Werra Uplift
We describe the Werra Anticline as a tectonostratigraphic unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein and Early Triassic. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:200000 of Thuringia, GK 1:300000 of Hesse. For References see also Tectonic boundaries in Germany.
Gelliehausen fault zone
The Gelliehausen fault is a NNE-SSW striking, narrow graben-like fault zone located predominantly within the western section of the Eichsfeld-Block with stratigraphic sequences of Middle Buntsandstein at the margins and deposits of Upper Buntsandstein and Lower Muschelkalk in the center of the fault zone. In the western Thuringian area this fault zone formed a narrow graben.
Rengelrode graben zone
The Rengelrode fault zone is a NNE-SSW striking narrow grabenin the southwestern section of the Eichsfeld Block with stratigraphic sequences of the Lower Muschelkalk as graben fill and deposits of the Middle Buntsandstein on the eastern flank and Upper Buntsandstein on the western flank.
southwestern fringe of the Bohemian Massif & the Thuringian Forest subdomains
It is an area under Mesozoic cover that is partly also uplifted but show also relicts of Jurassic in synforms and Upper Cretacous in foreland basins along the uplift of the Bohemian Massif. Several NW-SE striking Mesozoic fault zones (partly inverted) cross this structural unit and bound it in parts. The Northeastern part of this structural unit formed during the Late Cretaceous also belongs to the southern rim of the North German Basin.
We describe the southwestern fringe of Bohemian Massif & Thuringian Forest as a tectonostratigraphic unit, which is mainly influenced by uplift & denudation history of the Mid-German and Bohemian basement highs. The outline of this structural unit is mainly defined by the occurrence of basement uplifts under Mesozoic cover as well as the distributional pattern of Jurassic and Late Cretaceous. The northeastern border ist defined by the faults of the Franconian Lineament as well as the outcrops of Pre-Zechstein Basement. The transition to structural units to the West/Southwest is not always sharply defined. In the northwest, the Grabfeld flexure is a possible structure at which one could define the limit of the structural unit. The extent of this unit was newly created with a view to a structured assignment of generalized overview fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:200000 of Thuringia, GK 1:100000 of the Thuringian Forest (Kästner, 1996), GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996). For References see also Tectonic boundaries in Germany.
southwestern fringe of Bohemian Massif & Thuringian Forest
South Thuringian-Franconian fault zones & uplifts
We describe the South Thuringian-Franconian fault zones & uplifts as a tectonostratigraphic unit, whose boundaries are defined by faults and regional uplifts as well as the today's erosional pattern. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
Several NW-SE striking Mesozoic fault zones (partly inverted) cross this structural unit and bound it in parts. [Domain type: Basement uplifts under Mesozoic cover; Basement: Rhenohercynian/Saxothuringian/Moldanubian.]
Franconian Jurassic-Cretaceous Depression
We describe the Franconian Jurassic-Cretaceous Depression as a tectonostratigraphic unit, whose boundaries are only in sections defined by faults but also are defined on the base of distributional pattern of Cretaceous and Jurassic sedimentary successions. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
Domain type: Deformed sedimentary overburden, Basement: Moldanubian/Saxothuringian.
Vilseck Depression
We describe the Vilseck Depression as a tectonostratigraphic sub-unit of the Franconian Jurassic-Cretaceous Depression, whose boundaries are only in sections defined by faults but also are defined on the base of distributional pattern of the Late Cretaceous sedimentary successions. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
The Vilseck depression subdomain represents a Late Cretaceous foreland depression/graben and is located at the southwestern fringe of the Bohemian Massif. [Domain type: Late Cretaceous foreland basin, Basement: Moldanubian.]
Hollfeld-Veldenstein-Sulzbach-Kallmünz Depression
We describe the Hollfeld-Veldenstein-Sulzbach-Kallmünz Depression as a tectonostratigraphic sub-unit of the Franconian Jurassic-Cretaceous Depression whose boundaries are only in sections defined by faults but also are defined on the base of distributional pattern of the Late Cretaceous sedimentary successions. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
The Hollfeld - Veldenstein - Sulzbach - Kallmünz depression subdomain is located within the southwestern fringe of the Bohemian Massif and is characterized by the Hollfeld & Keilberg fault zone as the extension of the Bavarian Pfahl. [Domain type: Late Cretaceous foreland basin, Basement: Moldanubian/Saxothuringian.]
Bodenwöhr half-graben
We describe the Bodenwöhr half-grabens as a tectonostratigraphic unit (Late Cretaceous foreland Basin of the uplifted Bohemian Massif), whose boundaries are defined by faults as well as the distribution of Late Cretaceous sediments. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
The Bodenwöhr Half-graben subdomain is located within the southwestern fringe of the Bohemian Massif and is related to the Bavarian Pfahl. [Domain type: Late Cretaceous foreland basin, Basement: Moldanubian.]
Weiden Basin
We describe the Weiden Basin as a tectonostratigraphic unit (Late Cretaceous foreland Basin of the uplifted Bohemian Massif), whose boundaries are defined by faults as well as the distribution of Late Cretaceous sediments. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
The Weiden basin is located within the southwestern fringe of the Bohemian Massif and is related to the Franconian line. [Domain type: Late Cretaceous foreland basin, Basement: Moldanubian/Saxothuringian.]
Subhercynian Basin
We describe the Subhercynian Basin as a tectonostratigraphic sub-unit within uplifted parts of the North German Basin. The boundaries of the Subhercynian Basin are defined mainly by fault zones and faulted flexures as well as by outcop pattern made by deep erosion as a result of Late Cretaceous compression and uplift of this tectonic blocks. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-4000). Map Reference: Röllig et al. (1990), Beutler (2001), Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Beutler (2001), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
Strongly uplifted part of the North German Basin between the basement highs of Flechtingen-Roßlau in the north and the Harz in the south. The preserved Mesozoic sedimentary cover show mainly ESE/SE striking elements which have a Triassic extensional history and are later overprinted by Late Cretaceous contractional tectonics.
Subhercynian Cretaceous Basin
The Subhercynian Cretaceous Basin is a sub-unit of the Subhercynian Basin/depression. We describe the Subhercynian Cretaceous Basin as a tectonostratigraphic unit, whose boundaries are defined mainly by outcop pattern of Cretaceous north of the Harz Mountains. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-4000). Map Reference: Röllig et al. (1990), Beutler (2001), Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Beutler (2001), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
The Subhercynian Cretaceous Basin represents a Late Cretaceous foreland basin in front of the Harz Northern boundary fault. It is part of the Subhercynian Basin. [Domain type: Late Cretaceous forland basin, Basement type: Rhenohercynian.]
We describe the Egge-Kellerwald fault system as a fault system which separates the Münsterland Basin from the Hessian Depressian of the southern North German Basin. The cluster of sub-parallel faults in this region can sometimes reach several km to a few tens of km in width, and a discrete transition between the Hessian depression and the Münsterland Basin cannot be clearly defined along the entire fault system. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:300000 of Hesse, Baldschuhn et al. (2001), Ziegler (1990), GK 1:1000000 of Germany. For References see also Tectonic boundaries in Germany.
Egge-Kellerwald fault system
Predominantly N/NNW striking faults and Triassic grabens, with partially transpressive reactivation during Late Cretaceous times. The structural subdomain is characterized by a strongly deformed overburden. [Domain type: strongly deformed sedimentary overburden, Basement: mainly Rhenohercynian. Outcrop age: Triassic]
Fritzlar-Naumburg graben zone
We describe the Altmorschen-Neukirchen fault system as a fault system which separates the Thuringian Basin and the structures of the eastern Eichsfeld-Altmark Swell from the Hessian Depressian. The cluster of sub-parallel faults in this region can sometimes reach several km to a few tens of km in width and a discrete transition between the Hessian depression and the Münsterland Basin cannot be clearly defined along the entire fault system. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:300000 of Hesse, Baldschuhn et al. (2001), Ziegler (1990), GK 1:1000000 of Germany. For References see also Tectonic boundaries in Germany.
Altmorschen-Neukirchen fault system
NNE/NE Triassic faults and graben within the Hessian Trough/Depression. [Domain type: strongly deformed sedimentary overburden, Basement: Rhenohercynian. Outcrop age: Triassic]
North Hessian & Solling Block
We describe the North Hessian & Solling Block as a tectonostratigraphic sub-unit of the northern Hessian depression. The eastern and western boundaries of the Hessian Depression are today traced through larger fault systems. However, the actual structure has smooth transitions of paleofacial trends to neighbouring tectonostratigraphic blocks. In particular, the boundaries to the Lower Saxony Basin and to the Münsterland Basin cannot be clearly defined. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:300000 of Hesse, Baldschuhn et al. (2001), Ziegler (1990), GK 1:1000000 of Germany. For References see also Tectonic boundaries in Germany.
The North Hessian and Solling Block represents the transition between the North German Basin domain and the Hessian Trough/Depression. The block is characterized by few deformation and scattered faults and grabens. The structural subdomain is characterized by a deformed overburden and mainly Rhenohercynian basement. [Outcrop age: Triassic]
Falkenhagen Graben
Leinetal Graben
The Leinetal graben is a N/NNE striking Triassic (Keuperous?) graben, which was reactivated in Late Cretaceous times and presumably during the Cenozoic. The structural subdomain is characterized by a strongly deformed overburden and a Rhenohercynian basement. Outcrop age: Triassic
We describe the Leinetal Graben as a fault system in the northwest of the Hessian Depression. Even though the main structures of this region have been described in detail (e. g. Leiss et al. (2011)), no clear definition of the whole outline of this tectonic unit and associated fault system has been made to date. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:300000 of Hesse, Baldschuhn et al. (2001). For References see also Tectonic boundaries in Germany.
We describe the Southern Hessian Depression as a tectonostratigraphic sub-unit of the southern Hessian Depression/Trough. The structure has smooth transitions of paleofacial trends to neighbouring tectonostratigraphic blocks and is only partly bordered by faults. In particular, within this study the boundaries to neighbouring tectonostratigraphic units cannot be clearly defined. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: e.g. GK 1:300000 of Hesse, GK 1:1000000. For References see also Tectonic boundaries in Germany.
Southern Hessian Depression
The subdomain of the Southern Hessian Depression represents the less deformed part of the entire Hessian Depression and is characterized by partially slightly inverted Triassic grabens. The structural subdomain is characterized by a slightly deformed overburden and Northern Phyllite zone basement. [Outcrop age: Triassic, mainly BLower Triassic]
We describe the Prignitz-Lausitz-Riesengebirge Anticline as a tectonostratigraphic unit, whose boundaries are defined by faults and especially by distribution and outcop pattern of Mesozoic sedimentary successions at the Base of Tertiary and at the surface. The defined tectonostratigraphic unit lies within the two defined domains of the NGB (North German Basin - domain I: North German Plain & Central German North Sea / North German Basin - domain II: uplifted and/ or inverted southern regions of the North German Basin). Even though the main structures of this region have been described (e. g. Voigt., 2009), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: based on outlines from Röllig et al. 1990. Definition of outline is comprehensively described by Voigt (2009). Outlines recorded based on the circumscribing outcrop of Lower Cretaceous-Early Upper Cretaceous from Röllig et al. (1990) in the area of the North German Plain. To the southeast, the circumscribing outcrop of the Triassic around the Lusatian Block was followed (circumscribing also indicates uplift of the structure). Further to the SE, the boundaries of the basement unit Lusatian Block were traced, each of which is bordered by Upper Cretaceous basins. Uncertainties: Especially in the NW the unit is characterized by broad trend of a flat NW-SE striking anticline, which is not bordered by discrete structures. The extent is roughly derived from subsurface-outcrop maps. To the southeast, basement outcrops give no clear evidence for the underlying structure other than AFTA data, except for surrounding Upper Cretaceous foreland basins (see e.g. Voigt (2009)). Rough designation of overall structure in Voigt (2009). Individual structural elements are recorded in detail in Katzung & Ehmke (1993) and Franke (2020). For References see also Tectonic boundaries in Germany.
Prignitz-Lausitz-Riesengebirge Anticline
The NW-SE striking tectonostratigraphic domain of the Prignitz-Lausitz-Riesengebirge anticlinal zone is a summary of previously defined structural elements of the Tafeldeckgebirge and the basement that show similar development during Jurassic-Lower Cretaceous & Upper Cretaceous. A large number of the faults strike NW-SE, crossing elements such as the Triassic Rheinsberg Trough show NNE strike. The tectonostratigraphic domain describes an area characterized by Jurassic-Lower Cretaceous basin/graben formation as well as a Upper Cretaceous structural inversion (Voigt, 2009).Thereby this structure resembles in its development the Lower Saxony Basin or Broad Fourteens Basin. The southeastern area of the subdomain became more uplifted during the Upper Cretaceous than the remaining sections. The Saxony-Czech Cretaceous Basin (Elbkreide) adjacent to the south, proves the structural inversion along this subdomain. Towards the NW the amount of Cretaceous inversion decreases along the structure, so that in the northwestern area sediments of the Malm and Lower Cretaceous are still preserved. Domain type: Supra-regional uplift, Basement: Avalonia/Rhenohercynian/Saxothuringian/Moldanubian(?).
We describe the Rheinsberg Trough as a tectonostratigraphic unit of the North German Basin. It is a pre-existing early to middle Mesozoic sedimentary trough crossed by the later Jurassic to Cretaceous structure of the Prignitz Wall. It is only roughly outlined by the Mesozoic fault and salt structure pattern. Even though the main structures of this region have been described (e. g. Scheck & Bayer, 1999), no clear definition of the outline of this basin part has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: Scheck & Bayer (1999). The outline is the sum of the envelope of the areas with the highest Jurassic and Keuper thicknesses (Scheck & Bayer, 1999) and the NNE striking Triassic structural elements according to Doornenbal & Stevenson (2010). The Rheinsberg Trough designation is based on thickness maps after Scheck & Bayer (1999). Their data basis is not clearly shown. Likewise, the trough is only traced in thickness trends. Only with the present thickness trends together with the salt structures of the region and the faults shown in Doornenbal & Stevenson (2010) a coherent structural picture emerges. The blocks and lineaments defined by Beutler & Stackebrandt (2012) partly give a completely opposite structural picture. Although the existence of this structure is undisputed, its outlines have not yet been clearly depicted with certainty. For References see also Tectonic boundaries in Germany.
Rheinsberg Trough
Rheinsberg Trough subdomain
The subdomain of the Triassic to Jurassic Rheinsberg Trough runs transverse to the later developing structure of the Prignitz Wall. The general NW-SE alignment of the Prignitz Wall is interrupted in this area by a dominant NNE strike of the structures (faults, salt structures). [Domain type: Deformed sedimentary overburden, Basement: Avalonia/Rhenohercynian.]
Rheinsberg deep fracture
The 108 km long, NNW-SSW running Rheinberg deep fracture belongs to the Rheinsberg Trough and crosses to the Prignitz-Lausitz-Riesengebirge Anticline subdomain.
Prignitz Wall
We describe the Prignitz Wall as a tectonostratigraphic unit, whose boundaries are defined by faults and especially by the distribution and outcop pattern of sedimentary successions at the Base of Tertiary and at the surface. Even though the main structures of this region have been described (e. g. Voigt., 2009), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-1000). Map reference: based on outlines from Röllig et al. (1990). Outlines recorded based on the circumscribing outcrop of Lower Cretaceous-Early Upper Cretaceous from Röllig et al. (1990) in the area of the North German Plain. Especially in the NW the unit is characterized by broad trend of a flat NW-SE striking anticline, which is not bordered by discrete structures. The extent is roughly derived from subsurface-outcrop maps. Individual structural elements are named and described in Katzung & Ehmke (1993) and Franke (2020). For References see also Tectonic boundaries in Germany.
It is defined as a NW-SE elongated sedimentary high of Jurassic to Lower Cretaceous strata below Tertiary cover. Within this region Jurassic to Lower Cretaceous strata show partly higher thicknesses as the surrounding. Voigt (2009) interpreted this structure as an inverted Jurassic-Lower Cretaceous Basin /Graben which was inverted during the Late Cretaceous.
Groß-Köris-Merzdorf fault system
Groß Köris - Merzdorfer fault zone
The NW-SE running Groß-Köris-Merzdorf fault system is a ca. 100 km long, SW-dipping zone with associated salt structures in the East Brandenburg-North Sudetes depression within the thrusted Central North German basin. The fault system consists of several single faults.
Lausitz fault
Lausitz Escarpment
The NW-SE running Lausitz fault is a probably young paleozoic formed, several times reactivated deep fault located between the East Brandenburg-North Sudetes depression and the Prignitz-Lausitz-Riesengebirge Anticlinal zone in the SW. Within the SE-part this fault represents the separation between the variscian Paleozoic of the Görlitz Syncline and the young-paleozoic to mesozoic cover of the North Sudetes depression. The throw of the normal fault decreases in NW-direction continuously. Several NE-SW running faults interesect the Lausitz fault. Major activity is documented inbetween Buntsandstein and Upper Cretaceous times, younger activity is documented for Lower Miocene and only minor activity during post-Miocene.
Hoyerswerda fault
The NNE-SSW oriented and 29 km long Hoyerswerda fault is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain, and represents a prominent cross fault of the Lausitz fault (DE-635). Fault activity is documented up to the Cenozoic.
Schönewalde fault
The 58 km long, NW-SE running Schönewalde fault is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain. The SW-dipping fault shows throws of 100 to 200 m, recent reactivations are documented.
Wittenberg fault
The 106 km long, NW-SE oriented Wittenberg fault represents in the SE-part the border between the Prignitz-Lausitz-Riesengebirge anticline subdomain and the Halle-Wittenberg Block subdomain, and in the NW-part the border between the subdomains Altmark Fläming depression and Gardelegen-Flechtingen-Rosslau uplift. The Wittenberg fault is a listric, SW-dipping reverse fault, that was formed during inversion in Uppper Cretaceous times. Throws of up to >2000 m are documented.
Schweinitz fault
The 23 km long, NW-SE running Schweinitz fault is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain.
Potsdam fault
The 42 km long, W-E oriented Potsdam fault is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain, and is interpreted as the western extension of the Buckow fault. A fault throw between 250-300 m is documented.
Lower Elbe fault
Unterelbe fault
The 24 km long, WNW-ESE running Lower Elbe fault is located with the eastern part within the Prignitz-Lausitz-Riesengebirge Antinclinal zone and with the northwestern part within the Central North German Basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression). The fault is a listric, SW-dipping reverse fault that was reactivated in the course of Upper Cretaceous inversion.
Lausitz Block
A Basment High which is partly under Tertiary cover. The outcropping basement show mainly Variscan deformation. This Basement High is part and presumably the most uplifted part of the Late Cretaceous anticlinal uplift of the Prignitz-Lausitz-Riesengebirge Anticline. [Domain type: Variscan to Pre-Variscan basement block, Basement: Saxothuringian.]
We describe the Lausitz Block as a tectonic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein Basement. The extent of this tectonostratigraphic unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020)
Torgau-Doberlug Synclinorium
Torgau-Doberlug Synclinorium subdomain
The Torgau-Doberlug Synclinorium subdomain is one of structural elements that mantle the Bohemian Massif in the north. This subdomain show mainly Paleozoic rocks with Variscan age deformation and belongs to the Lausitz Block. [Domain type: Variscan basement block, Basement: Saxothuringian.]
We describe the Torgau-Doberlug Synclinorium as a tectonic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein Basement. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also Tectonic boundaries in Germany.
Finsterwald fault zone
The 36 km long, WSE-ENE oriented Finsterwald fault zone is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain.
Doberlug fault zone
The 32 km long, WSW-ENE oriented Doberlug fault is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain.
Großenhain fault
The 87 km long, NW-SE oriented Großenhain fault is is located within the Prignitz-Lausitz-Riesengebirge Anticline subdomain. While the fault is characterized by a 200 m wide ductile fault zone in the SE, the fault shows brittle deformation and high fracturing/joins in the NW.
Görlitz Synclinorium subdomain
Görlitz Synclinorium
The Görlitz Synclinorium is one of structural elements that mantle the Bohemian Massif in the north. This subdomain show mainly Paleozoic rocks with Variscan age deformation and belongs to the Lausitz Block. [Domain type: Variscan basement block, Basement: Saxothuringian.]
We describe the Görlitz Synclinorium as a tectonic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein basement. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), Existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also Tectonic boundaries in Germany.
Inner Lausitz fault
WNW-ESE oriented and 36 km long fault within the Prignitz-Lausitz-Riesengebirge Anticline subdomain. Fault throws of up to 800-1000 m are observed.
Mühlberg Depression
The Mühlberg depression subdomain represents an uplifted part of the North German basin. It represent Lower Triassic to Rotliegend remnants of the NGB and adjacent platform parts. It can be interpreted as a foreland syncline of an Upper Cretaceous active thrust. [Domain type: foreland syncline of a thrust fault, Basement: Saxothuringian.]
We describe the Mühlberg Depression as a tectonostratigraphic unit (erosional relict on top of basement high) whose boundaries are defined by faults and especially by outcop pattern of the Triassic as well as Zechstein and Upper Rotliegend. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also Tectonic boundaries in Germany.
Lausitz Anticlinorium
The Lausitz Anticlinorium is one of structural elements that mantle the Bohemian Massif in the north. This subdomain show mainly Paleozoic rocks with Variscan age deformation and belongs to the Lausitz Block. [Domain type: Variscan basement block, Basement: Saxothuringian.]
We describe the Lausitz Anticlinorium as a tectonic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein basement. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020)
Lausitz thrust
The 48 km long, WNW-ESE running Lusatian overthrust fault is located at the Prignitz-Lausitz-Riesengebirge Anticline subdomain and the Lausitz block therein. The SW-dipping reverse fault is characterized by Lower Cretaceous main activity and a throw of 500-1000 m.
Hessian Depression
Hessische Senke
Hessian Trough
Hessischer Trog
We describe the "Hessian Depression" as a tectonostratigraphic sub-unit within uplifted parts of the North German Basin. The East and West boundaries of the Hessian Depression are today traced through larger fault systems. However, the actual structure has smooth transitions of paleofacial trends to neighbouring tectonostratigraphic blocks. In particular, the boundaries to the Lower Saxony Basin and to the structures of the "süddeutsche Großscholle" cannot be clearly defined. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:300000 of Hesse, Baldschuhn et al. (2001), Ziegler (1990), GK 1:1000000 of Germany. For References see also „Tectonic boundaries in Germany”.
The Hessian Depression is a NNE-SSW elongated sub-basin of the NGB and is more or less aligned and controlled during the Triassic - Jurassic(?) by surrounding swells like the Eichsfeld-Altmark swell. As a result this sub-basin of the NGB show a Triassic basin evolution, as well as in parts graben tectonics (e.g. Leinetal Graben) and a Late Cretaceous contractional/transpressional overprint. The southern part of the Hessian Depression is also influenced by Tertiary evolution of the European Rift system and is parlty covered by Tertiary basin sediments. The region is also characterised by intense volcanic activity during the Tertiary period and is overlain in the south by the largest Tertiary volcanic complex known in Germany (Vogelsberg complex).
Gardelegen-Flechtingen-Rosslau Uplift
We describe the Gardelegen-Flechtingen-Rosslau Uplift as a tectonostratigraphic unit, whose boundaries are defined mainly by faultzones and faulted flexures as well as by outcop pattern made by deep erosion as a result of Late Cretaceous compression and uplift of this tectonic blocks. The Flechtingen-Rosslau Uplift is a strongly uplifted part of the Southern North German Basin basement on which minor synsedimentary deposits of the NGB have been preserved. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-3000, DE-ST-2000). Map Reference: Röllig et al. (1990), Beutler (2001), Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Beutler (2001), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
The Gardelegen-Flechtingen-Rosslau uplift domain belongs to the during the Late Cretaceous uplifed southern rim of North German Basin. [Domain type: Mixed basement and sedimentary cover, Basement: Rhenohercynian.]
We describe the Haldensleben-Wittenberg uplift as a tectonostratigraphic basement unit, whose boundaries are defined mainly by fault zones and faulted flexures as well as by outcop pattern made by deep erosion as a result of Late Cretaceous compression and uplift of this tectonic blocks. The Haldensleben-Wittenberg uplift is a strongly uplifted part of the Southern North German Basin basement on which no/minor synsedimentary deposits of the NGB have been preserved. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-2000, DE-ST-3000). Map Reference: Röllig et al. (1990), Beutler (2001), Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Beutler (2001), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
Haldensleben-Wittenberg uplift
Late Cretaceous basement uplift. The Mesozoic basin fill is only preserved in synforms that can be interpreted as foreland synclines in front of basement thrusts or faulted flexures. [Domain type: Variscan to Post-Variscan basement block, Basement: Rhenohercynian.]
Gardelegen uplift
We describe the Gardelegen Uplift as a tectonic unit, whose boundaries are defined mainly by fault zones and faulted flexures as well as by outcop pattern made by deep erosion as a result of Late Cretaceous compression and uplift of this tectonic blocks. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-2000). Map Reference: Röllig et al. (1990), Beutler (2001), Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Beutler (2001), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
Late Cretaceous basement uplift under Triassic cover. [Domain type: Basement uplifts under Triassic cover, Basement: Rhenohercyonian.]
We describe the Harz as a tectonostratigraphic basement unit, whose boundaries are defined by faults in the north and especially by outcop pattern of the Pre-Zechstein in the south. The Harz is a strongly uplifted part of the Southern North German Basin basement on which no synsedimentary deposits of the NGB have been preserved. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
Harz fault set
Harz Rhenohercynian
The Harz domain is a regional geological unit in the central section of the Rheno-Hercynian zone, which emerges from its environment of Late Paleozoic-Mesozoic-Cenozoic overlays as a horst-like Block running approximately orthogonal to the strike of the Variscan structures. A sharp boundary of the Harz domain is represented by the Harznordrand fault in the northeast, where it may have been overthrust by as much as 5-7 km, but at least 2-3 km, against the Subhercynian Basin. In the southeast, southwest and northwest, the boundary to the surrounding stuctural regions is characterized by unconformities of stratigraphic sequences of the Permosilesian molasse basement and Triassic on the Variscan basement. The Harz is the most prominent Late Cretaceous basement uplift of Mid-Germany. It is the result of NNE directed compression and the northern border fault of the Harz is the main fault of this anticlinal uplift. The Harz Nordrand fault is a steep south dipping basement fault and show partly characteristics of a faulted flexure. [Domain type: Variscan to Post-Variscan basement outcrop, Basement: Mainly Rhenohercynian, in SE Northern Phyllitic zone.]
Ilfeld Basin fault set
[Permo-Carboniferous basin; erosional relict. Domain type: Post-Variscan basement outcrop; Basement: Rhenohercynian.]
We describe the Illfeld Basin as a tectonostratigraphic basement sub-unit, whose boundaries are defined especially by outcop pattern of the Permo-Carboniferous. It lies on the Rhenohercynian basement rocks of the Harz. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
We describe the Northwestern Saxony Basement Block as a tectonostratigraphic basement unit, whose boundaries are defined by faults in the north and south as well as by outcrop pattern of the Pre-Zechstein. Besides basement outcrops of the Saxothuringian, the northwestern Saxony Basement Block show mostly outcrops of the Permo-Carboniferous Übergangsstockwerk. Northwestern parts of this block also represent uplifted basement of the NGB. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Franke (2020), Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also Tectonic boundaries in Germany.
Northwestern Saxony Basement Block
A basement high with Variscan to Post-Variscan outcrops which is mainly covered by Tertiary sediments. The uplift is the result of Late Cretaceous NNE directed compression. Fault strike: 1st order SE; 2nd order: ENE-NE/NNE
Landsberg-Naunhof fault
The 42 km long, NW-SE running Landsberg-Naunhof fault is located with the NW-part within the Halle-Wittenberg Block subdomain.
Marbach fault zone
Köthen-Bitterfeld fault
Köthen-Bitterfeld fault zone
The 67 km long, NW-SE running Köthen-Bitterfeld fault zone is located in the central part of the Halle-Wittenberg Block subdomain.
Bitterfeld-Wermsdorf fault
The 35 km long, WNW-ESE running Bitterfeld-Wermsdorf fault is located within the eastern part of the Halle-Wittenberg Block. In this area the Halle-Wittenberg Block shows the highest subsidence, and aside from Siliesian, Permian and Triassic sediments several NW-SE oriented graben-and synclines occur.
Halle fault
The 50 km long, WNW-ESE running Halle fault represents the border between the Merseburg block subdomain and the Halle-Wittenburg Block subdomain. This variscian fault was reactivated within Upper Jurassic to Cretaceous times. The northeastern located Halle-Wittenberg block was discplaced against the southwestern Merseburg block abouth 600 m, locally 1500 m.
Rötha fault
The 50 km long, WNW-ESE running Rötha fault is located at the border between the Northwestsaxonian Block in the northeast and the eastern part of the Thuringian Syncline in the southwest.
Halle-Wittenberg Block
The subdomain of the Halle-Wittenberg block is a basement high (mostly Permo-Carboniferous) under Tertiary cover. In the eastern part, a band of smaller half-grabens/synclines with Mesozoic and Upper Rotliegend fill runs along the boundary of the block. To the south, these structures are sharply demarcated (probably also foreland depressions of Upper Cretaceous uplifts and thus protected by erosion). Erosion of possibly up to 5 km, today partly under Tertiary cover. Domain type: Predominantly Variscan-to Post-Variscan basement block, partly Mesozoic strata is preserved within Late Cretaceous foreland foreland synclines; Basement: Saxothruringian, locally Mid-German Crystalline High.
We describe the Halle-Wittenberg Block as a tectonostratigraphic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Permo-Carboniferous under Tertiary cover. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), Beutler (2001), Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Beutler (2001), Martiklos et al. (2001). For References see also Tectonic boundaries in Germany.
Rosslau fault
The 25 km long, NE-SW runnig Rosslau fault represents within the pre-Cenozoic the border between the subdomains of the Rosslau-Gardelegen uplift and the Halle-Wittenberg Block. In this sense, the fault represents the boundary between the Northern Phyllite Zone in the northwest and the Mitteldeutsche Crystalline Zone in the southeast.
Halberstadt fault
The 20 km long, WNW-ESE running Halberstadt fault is located with the NW-part within the subhercynian basin subdomain and the the SE-part within the Halle-Wittenberg block subdomain.
Löbejün-Brehna fault
The 25 km long, WNW-ESE running Lobejün-Brehna fault is located within the southwestern part of the Halle-Wittenberg Block subdomain.
Bitterfeld Graben
Bitterfelder Graben
We describe the "Bitterfeld Graben" as a tectonostratigraphic unit (erosional relict on top of basement high) whose boundaries are defined by faults and especially by outcop pattern of the Triassic as well as Zechstein and Upper Rotliegend. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also „Tectonic boundaries in Germany”.
Permian to Lower Triassic sedimentary relict of the NGB. It can be interpreted as a Late Cretaceous thrust foreland depression. Outcrop age: Tertiary - Quaternary cover, Lower Triassic - Permian basin relicts; Basement: Saxothuringian - Mid-German crystalline High; partly covered by Permo-Carboniferous volcanics; fault strike: 1st order: SE / 2nd order: NE
Torgau fault system
The 40 km long, NNW-SSE running Torgau fault system is located within the northern part of the Halle-Wittenberg Block subdomain. To the south, this fault system is continued by the Großenhain fault.
Gräfenhainichen fault
The 63 km long, NW-SE running fault is located within the central part of the Halle-Wittenberg Block subdomain.
Düben Depression
Dübener Becken
We describe the "Düben Depression" as a tectonostratigraphic unit (erosional relict on top of basement high) whose boundaries are defined by faults and especially by outcop pattern of the Triassic as well as Zechstein and Upper Rotliegend. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also „Tectonic boundaries in Germany”.
Permian to Lower Triassic sedimentary relict of the NGB. It can be interpreted as a Late Cretaceous thrust foreland depression. Outcrop age: Tertiary - Quaternary cover, Lower Triassic - Permian basin relicts, Basement: Saxothuringian; partly covered by Permo-Carboniferous volcanics, fault strike: 1st order: ENE;E/SE / 2nd order: SSE/NNE
Thuringian Depression
The Thuringian Depression is an uplifted and deeply eroded marginal area of the North German Basin in Thuringia. During the Late Cretaceous (Santonian to Campanian) this basin part of the SPB/NGB (uplift after Beyer (2015) 1500 m to 3700 m) as well as the surrounding basement highs (uplift up to 5000 m and more) were uplifted. The main structure representing a NW-SE striking syncline, which is located in between the more strongly uplifted Variscian to Rotliegend basement of the Thuringian forest and Thuringian Schiefergebirge in the south and of the Palaeozoic outcrops of the Harz in the North (Fig. 9, Fig. 11 country sheet). The basin is limited in the West by the Eichsfeld-Altmark Swell and further west by NNE-SSW striking grabens (e.g. Leinetal Graben, Altmorschener Graben) within the northern Hessian Depression. To the NE the basin is limited by several smaller highs (Kyffhäuser, Bottendorfer Höhenzug) along the Kyffhäuser- Crimmitschauer fault zones. The uplifted basin part north of this fault zone is called the Mansfelder Mulde, which in turn is limited to the north by the Halle fault. Accompanying to the broad uplift of this region several NW-SE striking Late Triassic to Jurassic (maybe Early Cretaceous) small grabens were structurally inverted during the Late Cretaceous. Prominent examples for faults and fault zones are the Finne fault, the Kyffhäuser-Crimitschauer or the Eichenberg-Gotha-Saalfelder fault zone. These grabens and fault zones dominate with the exception of a few NNE-SSW striking elements (e.g. Ohmgebirge Graben) and WNW-ESE elongated minor oval uplifts the structural pattern of the Thuringian “Syncline.
We describe the Thuringian depression as a tectonostratigraphic unit, whose boundaries are defined by basement highs, faults & fault systems as well as of the Eichsfeld-Altmark Swell in the west. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-5000). For References see also Tectonic boundaries in Germany.
Zeitz-Schmölln depression
We describe the Zeitz-Schmölln depression subdomain as a tectonic sub-unit in the east of the Thuringian depression. The boundaries of the block only partially follow faults. Predominantly, the delineation is based on changes in the dip of the Thuringian depression. The unit corresponds to a 2nd order syncline with NW/WNW-SE/ESE strike. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the whole outline of this tectonic unit and associated fault system has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Strongly uplifted basin part of the NGB eroded down to the Lower Triassic. The WNW/NW-ESE/SE elongated synform is presumably the result of NNE directed Late Cretaceous contraction.
Crimmitschau fault zone
The 15 km long and NW-SE running Crimmitschau fault zone represents the southeastern section of the Kyffhausen-Crimmitschau fault zone (DE-536) and is located at the northern boundary of the Hermundurian Block. Reverse faults within the pre-Zechstein basement indicate weak compressions still in the Eocene. The fault zone belong to the supraregional Gera-Jáchimov fault zone.
Elstertal fault
The 15 km long, NNE-SSW running Elster fault is located within the southeastern part of the Merseburg Block and belongs to the subdomain of the Sangerhausen & Querfurt depression.
Sangerhausen & Querfurt depressions
We describe the Sangerhausen & Querfurt depression as a tectonic sub-unit of the Thuringian depression. The boundaries of the block only partially follow faults. Predominantly, the delineation is based on changes in the dip of the Thuringian depression. The unit corresponds to a 2nd order syncline. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the whole outline of this tectonic unit and associated fault system has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-5000). For References see also Tectonic boundaries in Germany.
Strongly uplifted basin part of the NGB eroded down to the Lower to Middle Triassic.
Kyffhäuser-Crimmitschau fault zone
The 56 km long and NW-SE running Kyffhäuser-Crimmitschau fault zone borders the Hermundurian Block in the south from the Merseburg Block in the north east. Associated faults are the Kyffhauser fault in the northwest and the Crimmitschau fault in the southeast. The fault zone is interpreted as northwestern Northeast-part of the supraregional Gera-Jáchymov zone.
Hornburg deep fault
The 61 km long, WSW-ENE running Hornburg Deep fault is predominantly located within the northern part of the Merseburg Block. At the SW-end the fault separates the Kyffhausen Block in the northwest from the Hermundurian Block in the southeast. The northeast border of the fault is found at the Halle fault, the southwestern end is represented at the Finne fault.
Blankenheim-Geiseltal fault
The 54 km long, WNW-ESE running Blankenheim-Geiseltal fault is located within the Merseburg Block and belongs to the subdomain of the Sangerhausen & Querfurt depression. Already in the Rotliegend this fault exerted influence on sedimentation or magmatic activities. She is a parallel fault to the Halle fault, which was also active in the Rotliegend.
Nebra fault
The 29 km long, NE-SW running Nebra fault is located within the central part of the Merseburg Block and belongs to the subdomain of the Sangerhausen & Querfurt depression. A surface-near observation is not possible.
Lauchstädt fault
The 16 km long, NW-SE running Lauchstädt fault is located within the northern part of the Merseburg Block, belongs to the subdomain of the Sangerhausen & Querfurt depression and shows a fault throw of up to 500 m.
Kyffhäuser Northeastern Boundary fault
The 33 km long, WNW-ESE runnig Kyffhausen NE-boundary fault is the western section of the Kyffhausen-Crimmitschau fault zone and is located at the northern boundary of the Hermundurian Block. At this fault together with the Kelbra fault the Kyffhausen mountains were uplifted successivly since the Upper Cretacous. The fault zones is interpreted as both normal and reverse fault, represents the northwestern end of the supraregional Gera-Jáchimov zone and is assumed to be the northwestward connection the the South Harz fault system. Furthermore, the fault is considered as a terrane boundary between the Central German Crystalline Zone and the Rhenoherzynian Zone.
Kelbra fault
The 20 km long, W-E-running Kelba fault is located at the northern boundary of the Hermundurian block and belongs to the subdomain of the Sangerhausen & Querfurt depression. Together with the Kyffhausen NE-boundary fault the Kyffhausen mountains were uplifted successively since Upper Cretaceous times.
Borna depression
We describe the Borna depression as a tectonic sub-unit in the east of the Thuringian depression. The boundaries of the block only partially follow faults. Predominantly, the delineation is based on changes in the dip of the Thuringian depression. The unit corresponds to a 2nd order syncline with NW/WNW-SE/ESE strike. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the whole outline of this tectonic unit and associated fault system has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Mansfeld Syncline
We describe the Mansfeld Syncline as a tectonic sub-unit in the north of the Thuringian depression. The tectonic unit boundaries are defined in the north and partly in the south by faults & fault zones. The unit corresponds to a 2nd order syncline with NW/WNW-SE/ESE strike. The demarcation to the tectonic blocks in the east and west can only be determined with uncertainty. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020), no clear definition of the whole outline of this tectonic unit and associated fault system has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-5000). For References see also Tectonic boundaries in Germany.
Strongly uplifted basin part of the NGB eroded down to the Middle Triassic. The syncline is the result of NNE directed Late Cretaceous contraction.
Hermundurian Block
We describe the Hermundurian Block as a tectonic sub-unit of the Thuringian depression, which borders the Thuringian Syncline in the north. The tectonic unit boundaries are defined by faults & fault zones and the orientation of the basement high. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the whole outline of this tectonic unit and associated fault system has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-5000). For References see also Tectonic boundaries in Germany.
The 10-12 km wide and 120 km Hermundurian Block was uplifted 600 m in Upper-Cretaceous to Cenozoic times, and borders in the south to the Thuringian syncline at the Finne fault and to the north at the Kyffhäuser NE-boundary fault, the Kyffhäuser-Crimmitschauer fault zone and the Crimmitschauer fault zone. [Domain type: Basement uplifts, partly under coverage; Basement: Northern Phyllitic zone/ Saxothuringian.]
Finne fault zone
The ca. 100 km long, WNW-ESE running Finne-Eisenberg fault zone represents the North eastern border of the Thuringian syncline. This very prominent, narrow fault zone expresses itself very differently in its course on the surface and in its structural style, sometimes it has an overthrusting character, sometimes flexure-like. The system of the Finne fault zone shows a nearly 100-km-long straight flexure that symbolizes the morphological and geological northeastern border of the Thuringian depression. The fault zone is up to 2 km wide and shows an average dip of 30°. In the central part, which should be surveyed here, the fault zone corresponds to a distinctive narrow band of highly deformed Triassic sedimentary rocks. The northwestern and especially the southeastern parts of the research area are developed as several parallel branch faults. In the southeastern elongation of the fault zone, which is not part of our survey, the sedimentary cover is missing. Here, it is possible to gain insight to the fact that the basement is also involved to the kinematics of the fault zone. The fault zone is interpreted also as northwestern Southwest-part of the supraregional Gera-Jáchymov-Zone.
Eisenberg-Pohlen fault zone
The Eisenberg-Pohlen fault runs NW-SE to WNW-ESE running fault zone within the eastern part of the Thuriningian syncline and southeastern part of the Finne-Eisenberg fault zone as well as central part of the overregional Gera-Jáchymov zone. The northwestern part shows thrust character.
NW Thuringian Depression (Ohmgebirge, Leinefeld Anticline, Bleicherode Depression)
We describe the NW Thuringian depression (Ohmgebirge, Leinefeld Anticline, Bleicherode Depression) as a tectonic sub-unit in the northwest of the Thuringian depression in the transition to the Harz Mountains. The boundaries of the block only partially follow faults. Predominantly, the delineation is based on changes in the dip of the Thuringian depression. The unit corresponds to a 2nd order syncline. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no definition of the here used/outlined higher-level structure in this form has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Strongly uplifted basin part of the NGB eroded down to the Middle Triassic. The Ohmgebirge graben as well as the minor anticlinal and synclinal structures are the result of Late Cretaceous contractional tectonics and partly of the inversion of Triassic structures.
Rengelrode graben fault zone
Ohmgebirge graben fault zone
The NNE-SSW striking Saxon Ohm graben fault zone is located in the NNW margin of the Thuringian depression and consists of the Worbiser Graben in the southwest and the Holunger Graben in the northeast. Significant is the evidence of Cenomanian sediments in both sections of the graben zone.
We describe the Thuringian syncline as a tectonic unit, whose boundaries are defined by faults & fault systems as well as of bordering basement highs. The Thuringian Syncline is part of the Thuringian depression. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the outline of this basin part has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Thuringian Syncline
The Thuringian Syncline as part of the Thuringian Depression is a during the Upper Cretaceous strongly uplifted part of the North German Basin. As a result of Late Cretaceous contractional tectonics this part of the NGB is uplifted at the northern and southern rim along steeply dipping basement thrusts and additionally the whole basin part was deformed to a broad ESE,SE-WNW/NW elongated Syncline. [Domain type: Deformed sedimentary overburden, Basement: Rhenohercynian/Saxothuringian.]
northwestern Thuringian forest border zone
We describe the northwestern Thuringian forest border zone as a highly deformed tectonic unit, which borders in the north the Thuringian forest. The tectonic unit boundaries are defined by faults & fault zones. The northwestern Thuringian forest border zone is part of the Thuringian depression. The defined unit was not described in this form before. Internal structural elements have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), but there exist no clear definition of the outline of this tectonic unit. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Uplifted southern parts of the Thuringian Syncline. Basement thrusts under Triassic cover or inverted grabens fringe the Thuringian forest in the north. The today's structural pattern is mainly the result of Triassic extensional tectonics and Late Cretaceous contractional tectonics.
Netra-Creuzburg Graben fault system
The Netra-Creuzburg Graben system represents a NW-SE elongated graben structure with its western section lying on Hessian territory. Here one of the few occurrences of the Rhaetian and Lower Jurassic deposits is found, which has been preserved within the Thuringian Depression. The structure is the western end member of the supra-regional Creuzburg-Ilmenau fault zone and consists of a complex system of numerous smaller grabens, horsts and faults. During the Late Cretaceous the graben is partly inverted and to the south is overthrusted by Paleozoic sediments and crystalline of the Thuringian Forest.
Thuringian Forest NE boundary fault
The Thuringian forest NE-boundary fault represents a NW-SE striking dislocation zone, probably initiated in Variscan or Pre-Variscan time and finally inverted or newly formed as major thrust/reverse fault, separating the Permo-Carboniferous of Thuringian Forest in the southwest from the Upper Paleozoic-Mesozoic platform cover of the Thuringian syncline in the northeast. The structural style of the fault is very heterogeneous and changes several times along the 30 km long running zone. In the west (Werra area), only a shallow flexure occurs, while towards southeast (Eisenach area) the flexure becomes steeper and changes into an reverse fault. At the northern edge of the so-called Ruhlaer Kristallin, a flexure occurs again, which further southeast again changes into an reverse fault.
Sättelstädt fault zone
The Sattelstädt fault is a 30 km long and NW-SE striking fault, which runs almost in extension of the Netra-Creuzburg graben fault system.
Sontra graben fault zone
Küllstedt fault zone
The Küllstedt fault zone is a NW-SE striking saxonic fault structure in the southeastern part of the Thuringian depression and is located on the northwestern margin of the Mühlhausen-Orlamünd Block. In the pre-Permian basement, it forms together with the Eichenberg-Saalfeld fault zone the northern occurence of equivalents of the Ruhla Crystalline and the Thuringian Main granite.
Kleinbucha fault zone
The Kleinbucha fault zone is a NW-SE striking saxonic fault zone consisting of several individual elements in the SSE area of the Thuringian Basin and forms the southeastern end member of the Erfurt-Kleinbucha fault zone. The fault zone is a graben structure with approximately 800 m segments. The total subsidence amounts to a maximum of 140 m. Likewise, deep drilling results do not exclude an already pre-Permian initiation of the fault zone.
Erfurt fault zone
The Erfurt fault zone is a NW-SE striking saxonic fault structure in the central section of the Thuringian depression and displaces the stratigraphic sequences of the Keuper in the northeast against series of the Upper Muschelkalk in the southwest. The fault zone appears as a horst structure, but partly also as a graben. Normal faulting often is observed on fault segments, and tectonic folding of higher order was found.
Schlotheim graben fault system
The NW-SE running Schlotheim graben fault system is located within the central part of the Thuringian depression. Aside from normal faults, also reverse faults are observed locally.The graben forms the southwestern end of the Kyffhäuser magnetic anomaly. The continuation of the Schlotheim Graben to the southeast is formed by the Ilmtal-Magdala-Leutraer Graben.
Ilmtal-Magdala-Leutra fault zone
The Ilmtal-Magdala-Leutra fault zone is located within the central part of the Thuringian depression, 40 km long and running NW-SE.
Leuchtenburg fault zone
The Leuchtenberg fault zone is located within the central part of the Thuringian depression, 27 km long and running WNW-ESE.
We describe the Eichenberg-Gotha-Saalfeld fault system as a fault system, whose boundaries are defined by faults & fault zones. The Eichenberg-Gotha-Saalfeld fault system is part of the Thuringian syncline. Even though the main structures of this region have been described in detail (e. g. Katzung & Ehmke, 1993; Franke, 2020; Seidel, 2003), no clear definition of the whole outline of this fault system has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Eichenberg-Gotha-Saalfeld fault system
The Eichenberg-Gotha-Saalfeld fault system is a WNW-ESE to NW-SE running complex fault system that extends over 130 km in centre of the Thuringian depression, from the Leinetalgraben in the west to the northern margin of the Thuringian Slate Mountains. The fault system was initiated in pre-Mesozoic times and was further formed in saxonian times, fault throw is about 500 m within the southwestern part of the Thuringian syncline. In the western section the fault system is characterized by a system of grabens, horsts and normal faults, while compressional elements are almost absent. Further southeast compressional structures, such as thrust and folds, occur until Arnstadt. At the SE-end thrusts dominate the fault zone. The extensional stage inbetween Triassic and Upper Cretaceous was followed by an compressional/transpressive stage in Santonina/Campanian times.
Remda fault zone
The Remda fault zone is a broad NW-SE striking saxonic fault structure in the southern part of the Thuringian syncline, often subdivided into a Northern Remda fault zone and a Southern Remda fault zone. Predominantly normal faults characterize the fault zone, only stronger compression have particularly affected the central part of the fault zone.
We describe the Thuringian Forest as a tectonostratigraphic basement unit, whose boundaries are defined by faults in the north and south as well as by outcop pattern of the Pre-Zechstein. The Thuringian Forest is a strongly uplifted part of the Southern North German Basin basement on which no/minor synsedimentary deposits of the NGB have been preserved. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:200000 of Thuringia, Franke (2020), GK 1:100000 of the Thuringian Forest (Kästner, 1996), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Seidel (2003). For References see also Tectonic boundaries in Germany.
Thuringian Forest fault set
Thuringian Forest
The Thuringian Forest is a Late Creataceous basement uplift covered with mainly Late Carboniferous to Lower Rotliegend continental redbeds and volcanics. In contrast to the Harz Mountains, the Thuringian Forest is bordered by Cretaceous reverse faults in the north as well as in the south (Franconian Lineament). In the NW the Ruhla crystalline represent Variscan partly high metamorphic basement outcrops.
Schiefergebirge nappe of Schmiedefeld Vesser
The allochthonous nappe of Schmiedefeld Vesser represents a part of the Thuringian Forest that belongs to the Thuringian-Franconian-Voigtland Schiefergebirge. [Domain type: Variscan basement block, Basement: Saxothuringian.]
We describe the Schiefergebirge nappe of Schmiedefeld Vesser as a allochthonous tectonostratigraphic basement unit on top of the basement unit of the Thuringian Forest. Its boundaries are defined by faults. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:250000 of Thuringia, Franke (2020), GK 1:100000 of the Thuringian Forest (Kästner, 1996), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Seidel (2003). For References see also Tectonic boundaries in Germany.
Ruhla Crystalline Complex
We describe the Ruhla Crystalline Complex as a crystalline basement unit within the northwestern Thuringian Forest. Its boundaries are defined by faults and discrete lithological change to the Permo-Carboniferous of the surrounding Thuringian Forest. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:250000 of Thuringia, Franke (2020), GK 1:100000 of the Thuringian Forest (Kästner, 1996), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Seidel (2003). For References see also Tectonic boundaries in Germany.
The Ruhla crystalline complex is a Variscan age basement outcrop of the NW Thuringian Forest. As the name suggests, this region is predominantly characterised by crystalline rocks, some of which are highly metamorphic. [Domain type: Variscan basement block, Basement: Saxothuringian- Mid-German Crystalline High.]
Klinger fault
Inselberg fault
Stahlberg fault
Heßleser fault
Franconian Lineament
Northern Kraichgau & Grabfeld Depression subdomain
We describe the Northern Kraichgau & Grabfeld Depression subdomain as a tectonostratigraphic unit, whose boundaries are only in sections defined by faults but also are defined on the base of partly fuzzy trends of the lithofacies and paleofacies. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
Northern Kraichgau & Grabfeld Depression fault set
The Northern Kraichgau & Grabfeld depression subdomain is characterized by inverted Mesozoic graben and a decrease of Late Cretaceous overprint towards SW within the subdomain. [Domain type: Deformed sedimentary overburden, Basement: Mainly Saxothuringian.]
transition North German Basin / Anglo Dutch Basin
Since no clear transition between the Anglo-Dutch Basin and the North German Basin can be defined (e.g. Geluk 2005, Doornenbal & Stevenson 2010, Wong et al. 2007), it is advisable to define a transition zone between the regions that can be clearly assigned to the respective basins. For the classification chosen here, all areas between Horn Graben and Central Graben and west of the line Ems lineament - Borkum fault - Harald lineament are assigned to this transition zone.
southwestern branch Horn Graben
"We describe here the "Southwestern branch of Horn Graben (Gerd Graben)" as a tectonostratigraphic unit whose boundaries are with the exception of the southern end are defined by faults and fault systems (e.g. the Nordschillgrund fault, Gernot fault, Weisse Bank Escarpment), but as well salt structures. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel 1995), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the ""transition region North German Basin/ Anglo Dutch Basin"" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001), and the structure of the Base Zechstein based on Baldschuhn et al. (2001). Outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021).
"The Southwestern branch of Horn Graben (Gerd Graben)" highlight the early structural evolution of the Horn Graben during the Lower and Mid-Triassic (SW-NE). During the Mid to Upper Triassic the Horn Graben then received its now dominant structural directions (N-S/SSE-NNW) (Jähne-Klingberg et al. 2018).
Schillgrund Platform
We describe here the "Schillgrund Platform" as a tectonostratigraphic unit whose boundaries are only in parts defined by faults and fault systems (e.g. the Nordschillgrund fault, Gernot fault, Weisse Bank Escarpment), but as well as partly fuzzy trends in the lithofacies and especially the distributional pattern of Mesozoic below the Late Cimmerian unconformity (Jakobsen et al. 2020). The region is less deeply eroded than the Schillgrund High and is still covered by Zechstein and Lower Triassic sediments as well as Mid-Triassic to Upper Triassic in the Dutch sector. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel 1995, Doornenbal & Stevenson 2010), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the ""transition region North German Basin/ Anglo Dutch Basin"" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. Both the transition to the Schillgrund Hoch and to the G+L Platform cannot be clearly defined. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001), Wong et al. (2007), and the structure of the Base Zechstein based on Baldschuhn et al. (2001). Outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021).
The Schillgrund Platform is characterized by subcrop of Triassic sediments below the Late Cimmerian unconformity, in parts already Kimmeridgian and Portlandian sediments (Kockel 1995, Jakobsen et al. 2020). The deep erosion in the area of the Schillgrund Platform is among other things the result of a large-scale uplift due to the formation of the North Sea dome (e.g, Doornenbal & Stevenson, 2010). The region shows predominantly salt pillows, but also isolated diapirs, whereby contrary to adjacent regions, the structures show only partial preferential directions.
Schillgrund High
We describe here the "Schillgrund High" as a tectonostratigraphic unit whose boundaries are only in parts defined by faults and fault systems (along the Nordschillgrund fault), but as well as partly fuzzy trends in the lithofacies and especially the distributional pattern of Mesozoic relicts below the Late Cimmerian unconformity. The region is more deeply eroded than the Schillgrund Platform but, in contrast to the adjacent East North Sea High to the north, is still covered by Zechstein sediments. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel 1995), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the ""transition region North German Basin/ Anglo Dutch Basin"" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001). Outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021).
The Schillgrund High is characterized by shallow position of the pre-Permian basement below the Late Cimmerian unconformity and by the subcrop of partly pre-Permian and thin Zechstein below the Early Cretaceous, in parts already Kimmeridgian and Portlandian sediments (Kockel 1995, Jakobsen et al. 2020). The deep erosion in the area of the Schillgrund High is the result of a large-scale uplift due to the formation of the North Sea dome but especially due to the rifting and rift-shoulder uplift of the Central Graben (e.g, Doornenbal & Stevenson, 2010). The demarcation to the Schillgrund Platform is rather vague.
G+L Platform
We describe here the "G+L Platform" as a tectonostratigraphic unit whose boundaries are defined both by faults and fault systems, salt structures as well as partly fuzzy trends in the lithofacies and thickness of stratigraphic units. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel 1995), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the "transition region North German Basin/ Anglo Dutch Basin" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), and the structure of the Base Zechstein based on Baldschuhn et al. (2001). Outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021). Uncertainties depend on whether the outline is drawn based on the structure of the top basement or the distribution of sediments and fault pattern in the overburden, there may be major differences (salt tectonics/tectonic decoupling).
A Mesozoic Platform area which is bounded to the east by the Harald Lineament and the Borkum Fault (Kockel 1995). The G+L platform is characterized structurally by the general subcrop of Middle Buntsandstein to Muschelkalk below the Late Cimmerian unconformity (Jakobsen et al. 2020), by the lack of major basement faults. Within the German North Sea sector this structural unit is bordered by long elongated salt-walls often in the near vicinity of major basement faults (e.g. Borkum fault). These salt walls, in turn, often have complex crestal fault systems. The demarcation to the Ameland & Schillgrund Platform is rather vague.
Anglo-Dutch Basin
We describe the "Anglo-Dutch Basin" as a sub-basin within the western Southern Permian Basin. Here we define this major basin as a tectonostratigraphic domain whose boundaries are not clearly defined by faults and fault systems. The outline of the domain can only be roughly defined based on lithostratigraphic trends and on the base of differences in the thickness and paleogeographical pattern of the Rotliegend and Zechstein. Even though the structure have been described (e. g. Geluk, 2005), no clear definition of the outline of this tectonostratigraphic unit has been made to date. Especially the border to the North German Basin can only be roughly defined but crosses/ is part of the tectonic sub-domains of the German North Sea sector. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The here used definition of the outline is based on a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future.
Although the Southern Permian Basin is often viewed as one basin, it is comprises three main tectonic units (Anglo-Dutch Basin, North German Basin, Polish Trough) as can be observed on the isopach map of the Rotliegend Sediments (Geluk, 2005). These three basins have a different origin; in part they are successor basins of the Variscan Foreland Basin, but mainly they represent new basins, which developed in response to latest Carboniferous to Early Permian wrenching/rifting and related volcanism. The Netherlands belongs to two of these basins. The NE onshore and northern offshore of the country belonged to the realm of the North German Basin, whereas the southern onshore and western offshore belonged to the Anglo-Dutch Basin (Geluk, 2005).
Central Graben
We describe here the "Central Graben" as a tectonostratigraphic unit whose boundaries are defined both by faults and fault systems, as well as partly fuzzy trends in the thickness and facies of stratigraphic units (Jakobsen et al. 2020). Even though the main structures of this unit have been described in detail (e.g. Arfai et al. 2014, Evans et al. 2003, Wride 1995), existing outlines of the large structure differ in part significantly. The main units of the Graben are: 1.) the Step Graben system with the Outer Rough Basin as well as adjacent minor horsts and grabens; 2.) the central deep subsided parts of the Graben system with the sub units: Tail End Graben, Dutch Central Graben, Salt Dome Province, the German John & Mads Graben, the German Clemens Basin and Clemens Graben. The extent of this tectonic domain was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. The Central Graben belongs to both the South Permian Basin in the area of the Anglo-Dutch Basin and the North Permian Basin. The graben also crosses the Mid/East North Sea - Rinköbing Fyn High. Uncertainties depend on whether the outline is drawn based on the structure of the top basement or the distribution of sediments and fault pattern in the overburden, there may be major differences (salt tectonics/tectonic decoupling).
The Central Graben is a half-graben that runs over 500 km S-N towards the Dutch, German, Danish as well as the British and Norwegian offshore sectors. Not least because of a comprehensive 3D seismic data coverage, the Central Graben represents the most explored one of the graben systems of the Southern and SE North Sea (Glückstadt Graben, Horn Graben, Central Graben), although, as it was affected by several different tectonic phases, it shows the highest structural complexity of the North Sea rifts. This high degree in structural complexity complicates the understanding of its structural evolution (Arfai et al. 2014, Thöle et al. 2021). In comparison to the Horn Graben & Glückstadt Graben, the Central Graben is the most developed half-graben with large listric fault systems at its eastern border (Nordschillgrund fault, Coffee Soil fault), while its less pronounced western flank (i.e. Step Graben system) is dissected in several smaller horst and grabens. Major tectonic subsidence activity in the Central Graben started in Keuper times, coinciding with renewed rise of activity in the Horn Graben and the Glückstadt Graben. However, there is also evidence of a Lower Triassic to Middle Triassic basin development, which probably did not lead to the formation of major faults. A second major phase of activity in the Central Graben lasted from the Upper Jurassic to the Lower Cretaceous, while in the Horn Graben only minor subsidence can be observed during this period. In the Late Cretaceous, the Central Graben was partly affected by structural inversion (e.g. Arfai et al. 2014), while the Horn Graben shows only minor renewed halotectonic activity with bulging of the roof of most of the salt diapirs.
Trier Bight & Gulf of Luxembourg domain
The Trier Bight & Gulf of Luxembourg domain contains a fault set of NE-SW oriented faults. The domain is characterized by Triassic overburden underlying Rhenish massif. [Domain type: Sedimentary overburden, Basement: Rhenohercynian.]
We describe the Trier Bight & Gulf of Luxembourg domain as a Mesozoic tectonostratigraphic unit on top of Rhenohercynian & Mid-German Crystalline High basement. The boundaries are defined by distribution of Jurassic to Upper Triassic sediments and the basement outcrops of the Rhenish Massif. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000, The Geological overview map of Rheinland Pfalz. For References see also Tectonic boundaries in Germany.
Saar-Nahe Basin domain
We describe the Saar-Nahe Basin as a tectonostratigraphic Permo-Carboniferous basement outcrop (or under Quaternary cover of the Northern Upper Rhine Graben) on top of Northern Phyllite Zone & Mid-German Crystalline High basement. The boundaries of this structural unit are defined by faults and especially by lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000. For References see also Tectonic boundaries in Germany.
The tectonic development of the Saar-Nahe Basin as a large Late Variscan molasse basin began simultaneously with the sedimentation of the oldest Upper Carboniferous (border between Namur and Westphalia) and was completed at the end of the Rotliegend. After Henk (1993) the basin is formed in the hanging wall of a major detachment which soles out about a depth of 16 km. The structural style of the basin is characterized by normal faults running parallel NE-SW oriented basin axis and orthogonal to this by transfer fault zones (Fig. 16b, country sheet). In the course of the postvariscan tectonic development older NE-SW striking faults seem to have been reactivated (Rein et al .2011). [Domain type: Post-Variscan basement block, Basement: Northern Phyllitic Zone & Saxothuringian to Mid-Crystalline High.]
Saar-Nahe Basin
The Upper Rhine graben belongs to the Cenozoic rift system (Ziegler 1992; ECRIS; see also Country Sheet) and predominantly is oriented NEE-SWW, in the line from Frankfurt to Basel. The graben is differentiated in three segments, each up to 100 km long (Grimmer et al. 2017). The evolution of the graben was controlled by multiple change of the stress field and a reactivation of Permo-Carbonifereous crustal discontinuities (Schuhmacher 2002). The formation and subsidence of the Upper Rhine Graben starts in the south during lower Eocene by NNW-SSE-extension, in the north during the Upper Eocene. The main rift stage began in the Lower Oligocene with continuous northward movements of the Alps (Dézes et al. 2004). During the early Miocene (Aquitanian), a major reorientation of the regional stress field is held responsible for the main subsidence phase of the northern parts of the Upper Rhine Graben. This is reflected by a counterclockwise rotation and northeastward shift of the depocenter axis and later by the middle Miocene uplift and erosion of the southern parts of the Upper Rhine Graben. The fault throw amounts to in the south about 5000 m and in the northern part above 4000 m. The offset of the eastern flank is up to 1000 m higher than on the western side. With rotation of the stress field from NNE-SSW within the Eocene before 6-7 Ma to NW-SO, transtensive strike-slip movements characterize the recent activity of the Upper Rhine graben. Today´s morphology of the flanks and the graben itself is characterized by great amount of normal faults or stepped faults and strike slip faults. After e.g. Derer et al. (2005) the fault pattern might be complex as illustrated in Fig. 13a (HIKE Country Sheet for Germany), where tilted fault blocks are bounded by growth faults. The complex, internal structural inventory of the graben is also revealed when looking at Fig. 13 b (Country Sheet), which Grimmer et al (2017) compiled and (re-)interpreted from numerous studies. The geological profile from the Saarland in the Northwest across the Upper Rhine graben, the Schwarzwald, Schwäbische Alb to the Alps gives an overview of the changing structural style in this part of Germany (Fig. 13c, Country Sheet; modified from Schreiner 2013). The NNE-SSW oriented major graben rim faults extend over a lenght of 209 km (DE-160) and 106 km (DE-161) respectively. [Domain type: Strongly deformed sedimentary overburden, Basement: Saxothuringian and Saxothuringian/Moldanubian.]
Upper Rhine Graben
We define here the Upper Rhine Graben as a superior Cenozoic tectonostratigraphic, unit, whose boundaries are defined by faults and fault systems, in particular by the distribution of thickened Cenozoic to Quaternary sedimentary successions. Partly the defined outline overlap with neighbouring tectonic units, because influence of rifting is also visible in adjacent basement highs and along the rift-shoulders. The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 300 of Hesse, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
Western segment subdomain
We define here the western segment subdomain as a Cenozoic tectonostratigraphic sub-unit of the Upper Rhine Graben, whose boundaries are defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. Partly the defined outline overlap with neighbouring tectonic units, because influence of rifting is also visible in adjacent basement highs and along the rift-shoulders. The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
N-S, NNW-SSE and NNE-SSW running faults within the western segment of the Upper Rhine graben. The length of the individual faults, with exception of the graben major faults, covers a range of ~ 10 to 30 km. The NNE-SSW oriented major graben rim faults extend over a lenght of 209 km (DE-160) and 106 km (DE-161) respectively. [Domain type: Strongly deformed sedimentary overburden, Basement: Saxothuringian/Moldanubian.]
Northern segment subdomain
We define here the northern segment subdomain as a Cenozoic tectonostratigraphic sub-unit of the Upper Rhine Graben, whose boundaries are defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. Partly the defined outline overlap with neighbouring tectonic units, because influence of rifting is also visible in adjacent basement highs and along the rift-shoulders. The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 300 of Hesse, GK 1000, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
N-S, NNW-SSE and NNE-SSW running faults within the western segment of the Upper Rhine graben. The length of the individual faults, with exception of the graben major faults, covers a range of ~ 10 to 30 km. [Domain type: Strongly deformed sedimentary overburden, Basement: Saxothuringian.]
Ilfeld-Bruchsal fault system
We define here the Ilfeld-Bruchsal fault system as a Cenozoic fault system of the Upper Rhine Graben, whose boundaries are defined by faults. Partly the defined outline can overlap with neighbouring tectonic units, because influence of rifting is also visible in adjacent basement highs and along the rift-shoulders. The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations, that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
The Ilfeld-Bruchsal fault system within the Upper Rhine Graben is characterized by predominantly NNE and subordinate SE-SSE and E-NNE striking faults. The length of the individual faults cover a range of ~ 10 to 30 km. The region of the Ilfeld-Bruchsal fault system shows a strongly deformed overburden and the basement belongs to the Saxothuringian/Moldanubian. [Main fault activity: Tertiary/Quaternary. Domain type: Strongly deformed sedimentary overburden, Basement: Saxothuringian/Moldanubian.]
Kaiserstuhl Block subdomain
We define here the Kaiserstuhl Block subdomain as a Cenozoic tectonostratigraphic sub-unit of the Upper Rhine Graben, whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions (in this case mostly volcanics). The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
The Kaiserstuhl Block within the Upper Rhingraben belongs to the Cenozoic volcanic complex (European Cenozoic Volcanic province), characterized by Tertiary/Quaternary main fault activity and subordinate fault activity during Jurassic, with NNE/N-S strike. [Domain type: Cenozoic volcanic complex, Basement: Moldanubian.]
We define here the southern segment subdomain as a Cenozoic tectonostratigraphic sub-unit of the Upper Rhine Graben whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
Southern segment subdomain
[Domain type: Stronlgy deformed sedimentary overburden, Basement type: Moldanubian.]
Eastern border zone subdomain
We define here the Eastern border zone subdomain as a Cenozoic tectonostratigraphic sub-unit of the Upper Rhine Graben, whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. Partly the defined outline overlap with neighbouring tectonic units, because influence of rifting is also visible in adjacent basement highs and along the rift-shoulders. The sub-domains here used are based on the classification of the GEORG project. The extent of the tectonostratigraphic domain was partly edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GeORG-Projektteam (2013). For References see also Tectonic boundaries in Germany.
The faults at the eastern border zone of the Upper Rhine graben show a predominanlty strike of NNE/NE and subordinate ENE/SE. Main fault activity is documented for Teritary-Quaternary, and subordinate for Triassic, Jurassic age. [Domain type: Strongly deformed sedimentary overburden, Basement: Saxothuringian/Moldanubian.]
Northern marginal area subdomain
Cenozoic-Quaternary marginal basins of the Upper Rhine Graben
We define here the Northern marginal area subdomain as a Cenozoic-Quaternary tectonostratigraphic sub-unit of the Upper Rhine Graben, whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GK 300 of Hesse. For References see also Tectonic boundaries in Germany.
Amöneburg Basin
Cenozoic-Quaternary sub-basin within the northern marginal areas of the Upper Rhine Graben. [Domain type: Sedimentary overburden, Basement: Rhenohercynian]
We define here the Amöneburg Basin as a Cenozoic-Quaternary sub-basin within the northern marginal areas of the Upper Rhine Graben, whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GK 300 of Hesse.
Mainz Basin
Cenozoic-Quaternary sub-basin within the northern marginal areas of the Upper Rhine Graben. [Domain type: Sedimentary overburden, Basement: Saxothuringian & Northern Phyllitic zone]
We define here the Mainz Basin as a Cenozoic-Quaternary tectonostratigraphic sub-basin of the northern Upper Rhine Graben, whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GK 300 of Hesse. For References see also Tectonic boundaries in Germany.
Hanau-Seligenstadt Basin
Cenozoic-Quaternary sub-basin within the northern marginal areas of the Upper Rhine Graben [Domain type: Sedimentary overburden, Basement: Saxothuringian, subordinated Northern Phyllitic zone.]
We define here the Hanau-Seligenstadt Basin as a Cenozoic-Quaternary sub-basin within the northern marginal areas of the Upper Rhine Graben, whose boundaries are partly defined by faults and fault systems, in particular by differences in thicknesses & facies of Cenozoic to Quaternary sedimentary successions. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 1000, GK 300 of Hesse. For References see also Tectonic boundaries in Germany.
Lower Rhine Bight
The NW-SE striking lower Rhine Bight, a recently seismically active, Cenozoic rifting zone, is bordered in the West and South by the Eifel and the Westerwald respectively, and rises up into the Rheinisches Schiefergebirge (Fig. 14a, HIKE country sheet for Germany). The formation of the still subsiding graben structure started in the Early Oligocene at around 36 Ma (Zijerveld et al. 1992) and therefore is younger than the Upper Rhine graben. Several major blocks and grabens characterize the area, each bounded by NW-SE striking faults, such as the Krefeld Block, the Köln Block, the Erft Block, the Peel Block as well as the the Roer Valley and Venlo graben (Fig. 14a, b, HIKE country sheet for Germany). According to Ahorner (1975) the initiation of rifting along NW-SE oriented basement faults probably was caused by a counterclockwise rotation of the regional stress field from NE-SW to NW-SE (Ahorner 1975). Recently recorded earthquakes indicate a stress field that is characterized by a subvertical σ1 and a subhorizontal NE-SW oriented σ3 indicating almost pure dip-slip for the predominately NW-SE striking normal faults (Hinzen 2003). Additionally to NW-SE striking fault zones and, to a lesser extent, WNW-ESE ones, large strike-slip faults characterize the recent structural style of the active graben. Highest fault offsets are found at the Erft and Rurrand faults with 100 -180 m (Hinzen 2003).
The extent of the Cenozoic tectonostratigraphic domain was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: e.g. Reicherter et al. (2008). For References see also Tectonic boundaries in Germany.
Erft Block
[Domain type: Strongly deformed Tertiary sedimentary overburden, Basement: Rhenohercynian.]
The extent of the Cenozoic tectonostratigraphic sub-domain was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: e.g. Reicherter et al. (2008). For References see also Tectonic boundaries in Germany.
Peel Horst
[Domain type: Strongly deformed Tertiary sedimentary overburden, Basement: Rhenohercynian/Avalonia(?).]
Roer Valley Graben subdomain
[Domain type: Strongly deformed Tertiary sedimentary overburden, Basement: mainly Rhenohercynian/Avalonia(?).]
Venlo graben
Krefeld Block
[Domain type: Deformed sedimentary overburden, Basement: Rhenohercynian/Avalonia(?).]
Cologne Block
South Limburg Block
Süd-Limburg-Block
The extent of the tectonostratigraphic sub-domain was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: e.g. Reicherter et al. (2008). For References see also „Tectonic boundaries in Germany”.
Rim of the Lower Rhine Bight. Only small parts of this structural unit are on German territory. Domain Type: sedimentary overburden; basement: Rhenohercynian; Outcrop age: 1st: L. Cret., Tertiary - Quaternary; 2nd: Paleozoic; Fault strike: SE/NE within basement /2nd: ESE
We describe the Merziger Graben & SW Saarland Triassic platform domain as a Mesozoic tectonostratigraphic unit east of the Trier Bight on top of the Permo-Carboniferous of the Saar-Nahe Basin (DE-963). The boundary in the NE is defined by outcrop pattern of the Triassic . A clear boundary to the Trier Bight (DE-961) and the Pfalz-Pirmasens-Nancy Trough (DE-964) is not recognizable. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000, The Geological overview map of Rheinland Pfalz. For References see also Tectonic boundaries in Germany.
Merziger Graben & SW Saarland Triassic platform domain
The Merziger graben & SW Saarland Triassic platform are located west of the Saar Nahe basin and contains a fault set with NNW-SSE and WSW-ENE running faults. The domain probably was a post-Triassic subsidence area. [Domain type: Sedimentary overburden, Basement: Saxothuringian.]
Pfalz-Pirmasens-Nancy Trough
The Pfalz-Pirmasens-Nancy trough is located at the French-German border close the the Upper Rhine graben domain, and presents a Triassic through structure. [Domain type: Sedimentary overburden, Basement: Saxothuringian-Mid-German Crystalline High.]
We describe the Pfalz-Pirmasens-Nancy Trough as a Triassic tectonostratigraphic unit, whose boundaries are defined by faults, the outcrop of the Saar-Nahe Basin in the north as well as based on partly fuzzy trends of the lithofacies and thickness of the Triassic. The extent of this structural unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK1000, The Geological overview map of Rheinland Pfalz. For References see also Tectonic boundaries in Germany.
Skurup Block
The Skurup Block is located within the Baltic Sea, is associated with the Teisseyre-Tornquist Zone and the Danish-Norwegian Basin. Domain type: deformed sedimentary overburden, Basement Domain: Baltica.
We describe the Skurup Block as a tectonostratigraphic unit, whose boundaries are only partly defined by faults. The outline of this tectonostratigraphic unit can be also defined based on lithostratigraphic trends. Even though the structure have been described (e. g. Seidel, 2019), no clear definition of the outline of this tectonostratigraphic unit has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Skurup fault
The NNW-SSE running Skurup fault close to the Danish border belongs to basement faults which are responsible for the stepwise southwestward dipping of Baltica (Seidel 2019).
Gat fault
The N-S running Gat fault close to the Danish border belongs to basement faults which are responsible for the stepwise southwestward dipping of Baltica (Seidel 2019).
Münsterland Cretaceous Basin
The Münsterland Cretaceous Basin is located south of the Lower Saxony Basin and is characterized mostly by nearly flat lying solid Upper Cretaceous limestones near the surface and residual preserved Lower Cretaceous, which lie directly on Paleozoic rocks. Due to Late Cretaceous inversion tectonics Upper Cretaceous sediments are thickened and strongly faulted in the vicinity of the Osning thrust system (northern border fault system). This basin area on the southern margin of the North German Basin was a sedimentary platform with only low subsidence rates for most of the Mesozoic. Presumably parts of this region were uplifted with the Rhenish Massif during the Jurassic. The bedding conditions of the Upper Cretaceous of the central Münsterland are considered relatively undisturbed (Dölling & Juch 2009). The rocks below the Upper Cretaceous (locally also Lower Cretaceous) form the coal-bearing strata of the Upper Carboniferous and are intensively folded as a result of the Variscan orogeny (Drozdzweski & Wrede 1994). The SW-NE striking Variscan folds are displaced by NNW-SSE striking cross faults, such as the Rheinpreußen or Fliericher Sprung, Sekundus-, Teritus- or the Drevenacker fault. [Domain type: Late Cretaceous foreland basin, Basement: Rhenohercynian/Avalonia(?).]
We define here the Münsterland Cretaceous Basin as a Late Cretaceous tectonostratigraphic unit, whose boundaries are defined both by faults and fault systems, partly fuzzy trends in the lithofacies and, in particular by the distribution of Cretaceous sedimentary successions. To the Lower Saxony Basin, the boundary of the basin runs along the Osning thrust. Because of that, the extent/outline of the Münsterland Basin overlaps with the extent/outline of the Lower Saxony Basin in this region. To the east this tectonostratigraphic unit overlap with the Egge - Kellerwald fault system (DE-1055). A discrete boundary cannot be clearly identified. But the extent to the west and south is defined by the today distribution of the Cretaceous. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: GK 200 (map-sheet 3902, 3910, 3918, 4702, 4710, 4718), Baldschuhn et al. (1996, 1997, 2001). For References see also Tectonic boundaries in Germany.
Münster fault
Schwelgern fault
Kurl fault
Haltern fault
Wilhelmine-Victoria fault
Alstätte fault
WNW-ESE running faults within the NW-part of the Münsterland Cretaceous Basin, close to the Dutch border.
Hervester fault
Wendfeld fault
Thyssen-Westende fault
Stadtlohn fault
Achenbach fault
Winterswijk fault
Königsborn fault
Öding fault
Flierich fault
Weseke fault
Sachsen fault
Drevenacker fault
Cenozoic impact Nördlinger Ries
The Nördlinger Ries structure is a Cenozoic (14.6 Ma) impact structure of 24 km in diameter, which is located between the Swabian and Franconian Alb.
German basement highs
Moldanubian basement domain
Variscan basement domain
The Bavarian-Bohemian Moldanubian subdomain belongs to the Bohemian Massif domain and is located at the southwestern rim therein. The subdomain is characterized by SE/ESE striking faults and Late Cretaceous-Tertiary uplift of the long-living basement high. [Outcrop age: Proterozoic, Domain type: Variscan basement block, Basement: Moldanubian.]
Bavarian-Bohemian Moldanubian fault set
Bavarian - Bohemian Moldanubian
We describe the Bavarian - Bohemian Moldanubian as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. It's a combination of the Moldanubian basement rock outcrops of the Bavarian Forest and the Bohemian Massif. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1531). For References see also Tectonic boundaries in Germany.
Black Forest domain
We describe the Black Forest domain as the sum of the outcropping Moldanubian basement unit, whose boundaries are defined by faults, lithological changes as well as the outcrop of Pre-Zechstein basement, but also as a broad strongly uplifted region along the eastern shoulder of the Upper Rhine graben (Black Forest uplift). The region of the Black Forest uplift overlap partly with other defined structural regions (DE-990, DE-989, DE-1025, DE-985). The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1000, geological overview map of Baden-Würtemberg, tectonic overview map of Baden Würtemberg. For References see also Tectonic boundaries in Germany.
This subdomain represents the part of the Black Forest domain which is characterized by strong Cenozoic uplift and Moldanubian (partially Saxothuringian) basement. SE/NNE/ESE-SE striking faults within the structural domain of the Black Forest. Outcrop age: Proterozoic-Paleozoic
Black forest basement high subdomain
Black forrest basement high
The Black Forest basement high subdomain represents the part of the Black Forest, which consists of outcropping pre-Zechstein basement (Moldanubian) and is characterized by predominantly SE/E-ESE striking faults. [Domain type: Variscan basement block, Basement: Moldanubian.]
We describe the Black Forest basement high as a outcropping Moldanubian basement unit, whose boundaries are defined by faults, lithological changes as well as the outcrop of Pre-Zechstein basement. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1000, geological overview map of Baden-Würtemberg, tectonic overview map of Baden Würtemberg. For References see also Tectonic boundaries in Germany.
Badenweiler-Lenzkirch fault system
The Badenweiler-Lenzkirch fault system within the Black Forest, which probably was active in Cenozoic times and represents a pre-Variscian suture zone. The subdomain is characterized by strongly deformed basement and ESE-SE/NNE striking faults. [Domain type: Strongly deformed basement, Basement: Moldanubian. Outcrop age: Proterozoic to Early Paleozoic]
We describe the Badenweiler-Lenzkirch fault system as a strongly faulted basement block within the Black Forest basement domain, whose boundaries are defined by faults & lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1000, geological overview map of Baden-Würtemberg, tectonic overview map of Baden Würtemberg . For References see also Tectonic boundaries in Germany.
We describe the Freiburg-Bonndorf-Bodensee fault system as a major fault system crossing the Black Forest, but strikes also more westward towards the Kaiserstuhl within the Rhein Graben and more eastward towards the Molassse Basin and the Hegau volcanic field. The boundaries of this strongly faulted block are defined by fault zones with mostly SE/ESE strike. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1000, geological overview map of Baden-Würtemberg, tectonic overview map of Baden Würtemberg. For References see also Tectonic boundaries in Germany.
Freiburg-Bonndorf-Bodensee fault system
The Freiburg-Bonndorf-Bodensee fault system is a Cenozoic active structural element with a main strike direction ESE/SE and is located in strike of Cenozoic volcanic fields. [Domain type: Mixed basement and sedimentary coverage, Basement: Moldanubian, Outcrop age: Proterozoic-Paleozoic, Triassic, Jurassic]
Saxothuringian basement domain
Elbezone
Variscan basement outcrops covered in parts by a Late Cretaceous foreland basin. This basement block borders the Erzgebirge to the SW and the Lausitz Block to the NW.
We describe the Elbe Zone as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), Franke (2020)
Saxonian Bohemian Cretaceous Basin
The Saxonian-Bohemian Cretaceous Basin represents a Cretaceous thrust foreland basin in the south of the uplifted Lausitz-Block. It lies on residual Triassic and Saxothuringian basement of the Saxony-Czech Elbe Zone. [Domain type: Late Cretaceous foreland basin]
The Saxonian Bohemian Cretaceous Basin is not part of the Saxothuringian basement domain of the Elbe Zone, but lies in the top of them. The here defined extent results from the today distribution of Upper Cretaceous sediments (Röllig et al. 1990, Katzung & Ehmke, 1993, digital GK 400 of Saxony).
Mügeln depression
The Mügeln Depression is not part of the Saxothuringian basement domain of the Elbe Zone, but lies in the top of them. The here defined extent results from the today distribution of Triassic to Late Permian sediments (Röllig et al. 1990, Katzung & Ehmke, 1993, digital GK 400 of Saxony).
The Mügeln depression represents a sedimentary Permo-Triassic relict surrounded in east and west by faults which are probably active during the Late Cretaceous. Those faults have partly Mesozoic to Paleozoic pre-cursors which are partly reactivated as reverse faults or define the strike of faults during Late Cretaceous. Because of wide-scale uplift and related intense erosion, Permo-Triassic remnants are often only preserved in the footwall of reverse faults. The Pre-Permian basement in the footwall of the Mügeln depression belongs to the Northwestern Saxony Basement Block and the Elbe Zone. The Permo-Triassic of this depression represents a rim facies of the North German Basin. This erosional relict is covered by Tertiary to Quaternary sediments. [Domain type: foreland syncline, Basement: Saxothuringian/ Permo-Carboniferous Post-Variscan basement unit]
Elbe Zone (Basement outcrops)
Basement outcrops
The basement subdomain of the Elbe zone domain is located at the northern rim of the Bohemian Massif, characterized by Saxothuringan basement and shows NW-SE running faults. [Domain type: Mixed basement and sedimentary coverage, Basement: Saxothuringian. Outcrop age: Paleozoic basement, Late Cretaceous, Neogene cover.]
We describe the Elbe Zone as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), Franke (2020). For References see also Tectonic boundaries in Germany.
Bohemian Massif & Variscan to Pre-Variscan fringe of the Bohemian Massif subdomain
Variscan basement outcrops
Fichtelgebirge fault set
We describe the Fichtelgebirge as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), HIKE (DE-BY_1531). For References see also Tectonic boundaries in Germany.
Fichtelgebirge
The Fichtelgebirge belongs to the Bohemian Massif domain and is located at the northwestern rim therein. The subdomain consists of Saxonthuringian basement and is characterized by SE-ESE striking faults. [Outcrop age: Proterozoic-Paleozoic, Domain type: Variscan basement block, Basement: Saxothuringian.]
Thuringian-Franconian-Voigtland Schiefergebirge fault set
We describe the Thuringian-Franconian-Voigtland Schiefergebirge as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. It's a combination of the Schiefergebirge units of Franconia, Thuringia & the Voigtland. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:200000 of Thuringia, GK 1:100000 of the Thuringian Forest (Kästner, 1996), GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), Röllig et al. (1990). For References see also Tectonic boundaries in Germany.
Thuringian-Franconian-Voigtland Schiefergebirge
The Thuringian-Franconian-Voigtland Schiefergebirge subdomain belongs to the Bohemian Massif domain and is located at the northwesternmost rim therein. The subdomain consists of Saxonthuringian basement and is characterized by SE-SSE/SSE striking faults. [Outcrop age: Ordovician-Carboniferous, Domain type: Variscan basement block, Basement: Saxothuringian.]
Granulitgebirge fault set
Granulitgebirge
The Granulitgebirge is one of structural elements that mantle the Bohemian Massif in the north. The subdomain consists of Saxonthuringian basement and is characterized by SE striking faults. [Outcrop age: Proterozoic, Domain type: Variscan basement block, Basement: Saxothuringian.]
We describe the Granulitgebirge as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also Tectonic boundaries in Germany.
Erzgebirge fault set
Erzgebirge
The Erzgebirge subdomain belongs to the Bohemian Massif domain and is located at the northern rim therein. The subdomain consists of Saxonthuringian basement and is characterized by prominent SE/NE striking faults. [Outcrop age: Proterozoic-Early Paleozoic, Domain type: Variscan basement block, Basement: Saxothuringian]
We describe the Erzgebirge as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020). For References see also Tectonic boundaries in Germany.
Gera-Jachimov fault system
Long living (Pre-Permian? - Permo-Carboniferous to Late Ctretaceous) fault system located within the Erzgebirge. The strongly deformed basement belongs to the Saxothuringian. [Outcrop age: Paleozoic, Domain type: Strongly deformed basement, Basement: Saxothuringian.]
We describe the Gera-Jachimov fault system as a strongly faulted block, whose boundaries are defined by faults. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Röllig et al. (1990), existing outlines: e.g. Franke (2020). For References see also Tectonic boundaries in Germany.
Tectonostratigraphic Permo-Caboniferous Übergangsstockwerk
Post-Variscan basement domain
Vorerzgebirge depression & Nossen-Wilsdruff Schiefergebirge
A basement high with Variscan outcrops
We describe the Vorerzgebirge depression & Nossen-Wilsdruff Schiefergebirge as a tectonostratigraphic basement unit, whose boundaries are defined by faults in the north and south as well as by outcrop pattern of the Permo-Carboniferous Übergangsstockwerk. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Franke (2020), Röllig et al. (1990), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020).
Hohenstein-Arnsdorf fault
Riechberg fault
Mid-German Crystalline High
Odenwald
The Odenwald domain represents a Tertiary uplift, is located at the NNE rim of the Upper Rhine graben and is characterized by NNE-SSW running faults. [Domain type: Mixed basement and sedimentary coverage/variscan basement block, Basement: Saxothuringian - Mid-German Crystalline High.]
We describe the Odenwald as a tectonostratigraphic basement unit, whose boundaries are defined by faults and the outcrop of the Pre-Zechstein. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:1000000 of Germany, GK 1:300000 of Hesse
Spessart
The Spessart basement high domain represents an uplifted/eroded part of the eastern shoulder of the Upper Rhine graben. [Domain type: Variscan basement block, Basement: Saxothuringian - Mid-German Crystlline High.]
We describe the Spessart as a tectonostratigraphic basement unit, whose boundaries are defined by faults and the outcrop of the Pre-Zechstein. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:1000000 of Germany, GK 1:300000 of Hesse
Rhenohercynian basement domain
Transition Harz - Halle-Wittenberg Block (Hettstedter Sattel)
A narrow W-E oriented basement high with mainly metamorphic rocks belong to the Phyllitic Zone and the Mid-German crystalline High
We describe the Transition Harz - Halle-Wittenberg Block (Hettstedter Sattel) as a tectonostratigraphic basement unit, whose boundaries are defined by faults and especially by outcop pattern of the Pre-Zechstein. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Martiklos et al. (2001), existing outlines: e.g. Katzung & Ehmke (1993), Franke (2020), Martiklos et al. (2001)
Teplá-Barrandium domain
Variscan Basement domain
Bohemian Massif
We describe the Bohemian (Teplá-Barrandium) block as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. It's a combination of the Tepla-Barrandium basement rock outcrops of the Bavarian Forest and the Bohemian Massif. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE-BY (<https://repository.europe-geology.eu/egdidocs/hike/7488_hike_fault_de-by_1494.jpg)
Variscan basement outcrop/high
Tirschenreuth-Mähring Zone
We describe the Tirschenreuth-Mähring Zone as a tectonostratigraphic basement unit (Teplá-Barrandium), whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE-BY (<https://repository.europe-geology.eu/egdidocs/hike/7488_hike_fault_de-by_1494.jpg)
Erbendorf-Vohenstrauss Zone
We describe the Erbendorf-Vohenstrauss Zone as a tectonostratigraphic basement unit (Teplá-Barrandium), whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations, that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE-BY (<https://repository.europe-geology.eu/egdidocs/hike/7488_hike_fault_de-by_1494.jpg)
We describe the Münchberg Crystalline complex as a tectonostratigraphic basement unit (Teplá-Barrandium), whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), HIKE-BY (<https://repository.europe-geology.eu/egdidocs/hike/7488_hike_fault_de-by_1494.jpg)
Münchberg Crystalline complex
The allochthonous Münchberg crystalline complex/nappe belongs to the Teplá-Barrandium and is located within the Bohemian Massif. [Domain type: Variscan basement block, Basement: Teplá-Barrandium]
Marienbad-Complex / Western Bohemian Shearzone / Teplá-Domazlice zone
Marienbad-Complex / Western Bohemian Shearzone / Tepla-Domazlice Zone
We describe the Marienbad-Complex / Western Bohemian Shearzone / Teplá-Domazlice zone as a tectonostratigraphic basement unit (Teplá-Barrandium) and major Basement Shear Zone whose boundaries are defined by faults and lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1531). For References see also Tectonic boundaries in Germany.
Domain type: Variscan basement block, Basement: Moldanubian.
The western and central part of the North German Basin (NGB) is characterized by a very complex pattern of grabens and structural highs, while the south is dominated by compressional structures. Due to pronounced overprint by salt tectonics, the causal tectonic influences on the structural genesis, however, is difficult to determine (Müller et al. 2016). The northern part of the NGB, especially in the German North Sea sector and in Schleswig-Holstein, is significantly influenced by the N-S-running Glückstadt Graben, Horn Graben and - in the very northwest - bordered by the Central Graben within the so called Entenschnabel area. The latter is moreover limited to the Central German North Sea by the North Schillgrund / Coffee Soil Fault. The formation of these large intracontinental rifts and the system of interconnected smaller Lower Rotliegend graben structures, as assumed by Gast (1988), is directly related in time to the disintegration of Pangaea and the development of large rift structures in the area of today's North Atlantic (i.a. Rockall-Faeroe Rift; Ziegler 1990). As structural highs, platform areas and sedimentary basin areas with only minor tectonics respectively, e.g. the Schillgrund High, G+L-Platform, the West Schleswig Block, the Mecklenburg Brandenburg Depression characterize the western and central part of the North German Basin. Towards the south, the structures of the German North Sea Sector and the Glückstadt Graben continuously merge into a not clear distinct structural region the Pompeckj Scholle (or Pompeckj Block). This Jurassic to Cretaceous platform to high is dissected by several, mostly already Triassic, fault zones, such as the Leer-Bremen Lineament or the Uelzen Lineament. As this structural region cannot be distinguished from neighboring parts of the basin in north-eastern Germany, neither in terms of facial nor structural aspects, the necessity of this structural division is questioned in recent literature (Müller et al., 2016). The fault zones within the Pompeckj Scholle (Pompeckj Block) have been reactivated several times during the Mesozoic. During the Upper Cretaceous pre-existing faults were locally compressive overprinted and basins and graben partly inverted (e.g. Bremen Graben) but to a much lesser extent than the adjacent Lower Saxony Basin to the south and associated structural features. Especially along the southern margin, grabens formed in the Jurassic (Lower Saxony Basin, Prignitz-Lausitz Basin). These were again inverted in the Upper Cretaceous, partly strongly uplifted and thus overthrust-related foreland basins were formed in the vicinity of these uplifts. Aside from these afore mentioned structural elements, a significant proportion of structural characteristics in the North German basin, especially in this western and central part, lays on salt structures and their associated faults. Compared to the western and central part of the NGB, the eastern section of the basin shows a clearly reduced structuring of the Mesozoic-Cenozoic overburden by halotectonic structures. In contrast to the western part of the NGB - with the exception of sections of the Altmark-Fläming Depression and the southwestern Mecklenburg-Brandenburg Depression - salt diapirs do not dominate here, but salt pillows. The northern and southern edges of this basin part are particularly markedly structured. Thus, in the north of the Mecklenburg Brandenburg Depression a system of prominent, NW/NNW-SE/SSE running fault zones has developed, which is also called the Vorpommern fault system (Krauss & Mayer 2004). The largest of these fault zones is the Möckow-Dargibeller fault zone, which is about 50 km long and show Early Cimmerian development (e.g. Gluško et al. 1976, Mayer et al. 2000). North of the Grimmen Wall, the NGB gradually changes to an elevated zone with significantly reduced Mesozoic-Cenozoic cover. The Møn-Arkona High (or Rügen Swell; Franke 1990, among others), in interaction with the Ringkøbing-Fyn High, has repeatedly been a swell region in CEBS' Paleozoic-Mesozoic development (Doornenbal & Stevenson 2010). In the outer NE of the German Baltic Sea sector runs the Skurup-Adler-Kamien fault, another important fault zone, which belongs to the Sorgenfrei-Tornquist Zone and the Teisseyre Tornquist Zone. The eastern part of the NGB merges to the east into the Szczecin-Kaliesz-East Brandenburg Swell (Ostbrandenburg Schwelle), which delimits the NGB from the eastwardly adjoining Wolsztyn High and Mid-Polish Trough. The North German Basin defined here traces in particular the outlines of the z1-z2 Zechstein Basin in the area of northern and central Germany. Some boundaries can only be vaguely defined due to strong erosion along the northern and southern margins of the basin. The term North German Basin is also used in a geomorphological context. In this specific case it would roughly correspond to the contiguous distribution of Cenozoic sediments. For a clearer assignment of the sub-domains to zones of the same or similar genesis, at least episodically, we divide the North German Basin into a part that is still characterised by a lowland plain and lies under Mesozoic and Cenozoic cover and a part that was strongly uplifted during the Upper Cretaceous and Cenozoic and is characterised by deep erosion, whereby this region is today interspersed with basement outcrops/highs. The main fault characeristics are: normal dip slip faults/extension; most of the Mesozoic and Cenozoic time strike-slip movement is subordinate or/and focused on a few prominent lineaments; along the southern rim often dip-slip inverted features; partly Late Cretaceous strike-slip tectonics along N to NNW striking faults; transtensional Rotliegend faults; mainly thin-skinned tectonics in the Mesozoic Supra-Salt overburden; most of faults in the Mesozoic to Cenozoic overburden are influenced by halotectonic processes (salt walls and diapirs).
We define here the North German Basin - domain I as a tectonostratigraphic unit, whose boundaries are defined both by faults and fault systems, often fuzzy trends in the lithofacies and, in particular by the expression of deformation events. The division into two domains of the North German Basin (NGB) is intended to indicate in particular the uplift of some basin regions during the Late Cretaceous and the associated different levels of erosion in this region. Depending on the level of erosion and the preservation of signs of former deformation phases, this results in regionally partly different dominant fault patterns, even if these deformation phases have influenced almost the entire basin. The Lower Saxony Basin, which was actually also strongly inverted during the Late Cretaceous, should therefore actually be part of domain II of the NGB: uplifted and/ or inverted southern regions of the North German Basin. However, it is also largely part of the German lowlands. In this respect, the subdivision made here should only be understood as a rough classification. The extent of the tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described or discussed in detail in the future. For References see also Tectonic boundaries in Germany.
North German Basin - domain I: North German Plain & Central German North Sea
West Schleswig Block
We describe here the "West Schleswig Block" as a tectonostratigraphic unit whose boundaries are defined both by faults and fault systems, salt structures as well as partly fuzzy trends in the lithofacies and thickness of stratigraphic units. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel, 1995), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the "North German Basin" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Outline definition is redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001), and the structure of the Base Zechstein based on Baldschuhn et al. (2001) & Doornenbal & Stevenson (2010) and is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021) observed major offsets in the base Zechstein as well as high thicknesses of the Keuper, Buntsandstein. Uncertainties depend on whether the outline is drawn based on the structure of the top basement or the distribution of sediments and fault pattern in the overburden, there may be major differences (salt tectonics/tectonic decoupling).
Following Kockel (1995), this unit covers the greatest part of the German North Sea sector. lt is bordered in the west and southwest by the salt structures Erika-Dina-Hilde-Helma-Hannelore, Heike, Hilda Nord-Hilda Süd and Herta-Halla-Lollo. The southern border runs from Julia and Jasmin to Jette and north of Johanna, Josephine and Feuerschiff Elbe I to the Eiderstedt peninsula. In the north, the southern margin of the Ringköbing-Fyn High borders the West Schleswig Block and in the east the Oldenswort - Mildstedt salt structure. In the SW a narrow promontory, characterized by the salt pillows Henni, Henni Nord and Hulda reaches the Harald Lineament, which belongs to the Horn Graben system. The West Schleswig Block is characterized structurally by the general subcrop of Keuper or Muschelkalk-Upper Buntsandstein below the Late Cimmerian unconformity, by the lack of major basement faults and the absence of salt diapirs. A few basement faults of minor importance parallel to the eastern Horn Graben boundary fault have been observed in the west, straddled by the salt pillows Elisa, Jutta and Helen. In the east, basement faults again occur below the Rochelsteert salt pillow. The rest of the West Schleswig Block is exceptionally little deformed. The broad, very flat salt pillows do not show any preferred direction. The salt movements into the sa!t pillows on the West Schleswig Block began by pre-Early Cretaceous times in most cases and often continued during the Late Cretaceous and Early Tertiary. The Helgoland salt pillow has not yet reached the diapiric stage and only a crestal graben originated in post-Middle Miocene times (BINOT 1988, 1991). In the context of the entire North German Basin, the WSB can rather be regarded as a sediment platform most of the time without major fluctuations in the thickness distribution of the Mesozoic.
southern branch Horn Graben
We describe here the "southern branch of the Horn Graben" as a tectonic unit whose boundaries are defined both by faults and fault systems, salt structures as well as partly fuzzy trends in the thickness of stratigraphic units. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel, 1995), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonic sub-domain of the "North German Basin" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001), and the structure of the Base Zechstein based on Baldschuhn et al. (2001). The outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021). Uncertainties depend on whether the outline is drawn based on the structure of the top basement or the distribution of sediments and fault pattern in the overburden, there may be major differences (salt tectonics/tectonic decoupling).
This southern extension of the Horn Graben developed from the Middle to the Upper Triassic. The Harald Lineament, the Hanno & Heiner Escarpment connect the northern extensions of the Ems Lineament with the central part of the Horn Graben. The interplay of rifting and reactive diapirism led to the formation of assymetric diapirs and salt mini-basins and was described by Thieme & Rockenbauch (1999) as example for raft tectonics.
Horn Graben
We describe here the "Horn Graben" as a tectonostratigraphic unit whose boundaries are defined both by faults and fault systems, salt structures as well as partly fuzzy trends in the lithofacies and thickness of stratigraphic units. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel, 1995, Best 1983), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the "North German Basin" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001), and the structure of the Base Zechstein based on Baldschuhn et al. (2001). Outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021) observed major offsets in the base Zechstein as well as high thicknesses of the Triassic (esp. Middle Buntsandstein and partly Mid-Triassic). Uncertainties depend on whether the outline is drawn based on the structure of the top basement or the distribution of sediments and fault pattern in the overburden, there may be major differences (salt tectonics/tectonic decoupling).
The Horn Graben is the most prominent structural element of the Central German North Sea. It is a up to roughly 10000 m deep aborted rift with the main activity during the Triassic. The graben show besides halotectonic mobilization of thick Zechstein salt also the mobilization of Upper Rotliegend formations (Jähne-Klingberg et al. 2018b). The Horn Graben shows similarities but also clear differences to the neighbouring rifts (Central Graben & Glückstadt Graben) (Jähne-Klingberg et al. 2018).
We describe the Central North German Basin as a tectonostratigraphic sub-domain of the North German Basin whose boundaries are not clearly defined by faults and fault systems. The outline of the domain can only be roughly defined based on lithostratigraphic trends and on the base of differences in the deformation pattern to surrounding areas. Even though the main structures, Basin Centre within the Northwestern part of the North German Basin / the West-Mecklenburg Block / The Mecklenburg-Brandenburg Depression, of this region have been described in detail (e. g. Baldschuhn et al., 2001; Katzung & Ehmke, 1993), no clear definition of the outline of this basin part has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-1000). Definition of the outline: deepest parts of the North German Basin basin outside of grabens (e.g. Glückstadt Graben) were summarized as well as areas with low deformation in the Mesozoic-Cenozoic overburden and only minor offsets at the base Zechstein. Uncertainties: The following transitions cannot be clearly defined because they are not tied to discrete structures: 1.) Transition to the east to the element eastern rim NGB, 2.) Transition to the NE to the element northeastern rim NGB, 3.) Transition to the Prignitz Wall (an anticline with major erosion in the top), 4.) Transition to the East Brandenburg-North Sudetes depression, 5.) no clear delineation in the deepest basin regions between the Central North German Basin and the southward trending Glückstadt Graben. For References see also Tectonic boundaries in Germany.
Central North German Basin
The Central German basin subdomain is defined by several grouped blocks (defined in the GTA) in the central, deeply subsided area of the NGB. It is characterized by thermal subsidence and no clear overprinting by Upper Cretaceous contractional tectonics. In the eastern part of the basin, many ESE/SE longitudinally elongated salt structures occur (presumed relation to raft-tectonics), and it is also characterized by fewer diapirs or salt walls than in the surrounding structural areas. Large regions in the western and central parts are characterized by deep ablation before and during the Upper Jurassic and deepest Lower Cretaceous, as well as deposition of only low thickness marine younger Lower Cretaceous and a thick Upper Cretaceous cover. This typical Tectonostratigraphy is also summarized under the name Pompeckj block. In addition to a generally low degree of structuring, the subdomain is characterized by relatively high stratiform salt thicknesses of the Zechstein and Oberrotliegend. Embedded in the eastern basin part, the NNE striking Rheinsberg Trough crosses the subdomain (could also be considered part of the central basin part. Map reference: redefined and summarized from Baldschuhn et al. (1996) (esp. structural maps and profiles), Baldschuhn et al. (1997) & Katzung & Ehmke (1993), and base Zechstein from Doornenbal & Stevenson (2010). [Domain type: Sedimentary overburden, Basement: Avalonia/Rhenohercynian.]
Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression
The Center of the NGB can be subdivided in three sub-domains (Basin Centre within the Northwestern part of the North German Basin / the West-Mecklenburg Block / The Mecklenburg-Brandenburg Depression). Those can be described as tectonostratigraphic sub-domains of the North German Basin, whose boundaries are not clearly defined by faults and fault systems. The outline of the sub-domains can only be roughly defined based on lithostratigraphic trends and on the base of differences in the deformation pattern to surrounding areas. Even though the main structures of this region have been described in detail (e. g. Baldschuhn et al., 2001; Katzung & Ehmke, 1993), no clear definition of the outline of this basin part has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Salzwedel fault
The western part of the 74 km long, WNW-ESE running Salzwedel fault is located at the northern rim of the Altmark-Fläming depression and merges with the Central North German Basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression) in the eastern part. This listric fault is a southwest dipping reverse fault that was reactivated during Uppper Cretaceous inversion.
Berdum-Jaderberg-Sagermeer fault
The 93 km long, NNW-SSE running Berdum-Jaderberg-Saagermeer fault zone is located with the southern part in the Südoldenburg-Hoya block (the thrusted part of the Central North German basin) and in the northern part within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression). Associated with this fault zone are the salt structures Saagermeer, Jaderberg and Berdum-Jever.
Bedekaspel-Marga fault zone
The 21 km and respectively 37 km long, N-S oriented Bedekaspel-Marga fault zone is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression).
Uelzen lineament
The 126 km long, NW-SE Uelzen fault zone is running at the northern rim of the Rotenburg-Soltau-Eldingen block, which belongs to the thrusted part of the Central North German basin, an runs further north into the Central North German Basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression). In the southern section this fault zone was involved in the sedimentary and structural development of the Eichsfeld Altmark swell. Above this fault zone synsedimentary grabens, horsts, and half grabens originated in the Early Triassic rocks.
Quickborn fault
The 23 km long, N-S oriented Quickborn fault is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression), close to the Glückstadt graben subdomain.
Stade-Langenfeld fault zone
The 55 km long, WNW-ESE oriented Stade-Langenfeld fault zone is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression), close to the Glückstadt graben subdomain.
Witzhave-Segeberg-Plön fault zone
The 94 km long, N-S oriented Witzhave-Segeberg-Plön fault zone is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression), close to the Glückstadt graben subdomain.
Bahlburg-Hohenhorn fault zone
The 70 km long, NNE-SSW oriented Bahlburg-Hohenhorn fault zone is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression) and borders to the thrusted part of the basin - the Rotenburg-Soltau-Eldingen Block.
Moisburg-Reitbrook fault zone
The 41 km long, WSW-ENE oriented Moisburg-Reitbrook fault is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression).
Lübtheen-Camin fault
The 42 km long, N-S oriented Lübtheen-Camin fault is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression).
Strackholt-Langeoog-Mira fault zone
The 57 km long, N-S oriented Strackholt-Langeoog-Mira fault zone is located within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression) and is characterized by normal faults within the overburden of the associated salt diapirs.
Arendsee Deep fracture fault
The 28 km/18 km long, NNE-SSW running Arendsee deep fracture fault is a basement fault located within the NW-part of the Altmark-Fläming depression of the thrusted Central North German Basin and within the Central North German Basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression) respectively. The southern part of the fault also is associated with the Eichsfeld-Altmark swell.
Gudow-Gülze-Sumte fault zone
The 32 km long, NNW-SSE oriented Gudow-Gülze-Sumte fault zone is located within the eastern area of the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression).
Rockenthin fault
The 8 km long, NNE-SSW running Rockenthin fault is located at the southern tip within the Altmark Fläming depression of the thrusted Central North German Basin and at the northern part within the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression) and the Eichsfeld-Altmark swell. Fault activity already observable during Triassic times, main activity of the reverse fault during Upper Cretaceous and related graben structures show Lower Cretaceous infill.
Oldendorf-Adolphsdorf fault zone
The 35 km long, NNW-SSE oriented Oldenforf-Adolphsdorf fault zone is located within the western area of the Central North German basin (Central NWGB - Ostholstein-West-Mecklenburg Block - Mecklenburg-Brandenburg Depression).
East Frisia – Ems Estuary Region
We describe here the "East Frisia – Ems Estuary Region" as a tectonostratigraphic unit whose boundaries are defined both by faults and fault systems, salt structures as well as partly fuzzy trends in the lithofacies and thickness of stratigraphic units. Even though the main structures of this unit have been described in detail (e.g. Kockel et al. 1991, Kockel, 1995), no clear definition of the outline of the structural unit has been made to date. The extent of this tectonostratigraphic sub-domain of the "North German Basin" was newly created with a view to a structured assignment of fault data and the assignment of an uniform structural history for this sub-domain. The outline is based on the analysis of a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (2001), and the structure of the Base Zechstein based on Baldschuhn et al. (2001). Outline definition is especially related to the profiles of the GTA (Baldschuhn et al. 1996) and existing 3D models (BGR, 2021). Uncertainties depend on whether the outline is drawn based on the structure of the top basement or the distribution of sediments and fault pattern in the overburden, there may be major differences (salt tectonics/tectonic decoupling).
This structural region lies in the northern extension of the Ems Lineament. Five NNE striking fault systems with associated salt walls cross and border this structural region.
We describe here the Glückstadt Graben as a tectonostratigraphic unit, divided into 7 blocks, whose boundaries are defined both by faults and fault systems as well as partly fuzzy trends in the lithofacies. Even though the main structures of this basin have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of the graben and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the North German Basin was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. For References see also Tectonic boundaries in Germany.
Glückstadt Graben
The Glückstadt Graben subdomain represents an aborted intracontinental rift and deepest of Mesozoic rifts in the Southern Permian Basin. The subdomain is characterized by high thicknesses of the Buntsandstein, Keuper and younger Mesozoic sediments in the rim synclines of salt walls. Moreover, intensive salt tectonics with intensive mobilization of the thick Rotliegend salinar are observed (References: e.g. Warsitzka et al. (2016)). [Domain type: Deformed sedimentary overburden, Basement: Avalonia]
We describe here the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Graben as a separate tectonic block of the Glückstadt-Graben, whose boundaries are defined both by faults and fault systems as well as salt walls. Even though the main structures of this region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of the tectonic unit and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Graben was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Outline definition: a) Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). b) Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. c) NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Uncertainties: Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. For References see also Tectonic boundaries in Germany.
Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Graben
The subdomain of the Southern Glückstadt Graben/Krummendeich-Hohenlockstedt Block represents a summary of southern parts and already defined blocks of the Glückstadt graben with similar characteristics. In this region, the dominant structural trend with NNE strikes is disturbed by ESE striking cross elements. From there, the impression of undulating salt structures in the overburden is created. Bounded to the east by the Emtinghausen-Krautsand lineament. [Domain type: Deformed sedimentary overburden, Basement: Avalonia.]
Krempe-Lägerdorf fault zone
The 41 km long, WSW-ENE oriented Krämpe-Lägerdorf fault zone is located within the region of the Eastern and Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Block and belongs superordinately to the Glückstadt graben subdomain.
Sushörn fault
The 29 km long, WNW-ESE oriented Sushörn fault belongs superordinately to the Glückstadt graben subdomain, and is located with the southern part within the region of the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Block and with the northern part within the western branch of the Glückstadt graben.
Süderhastedt-Sieverstedt fault zone
The 60 km long, NNE-SSW oriented Süderhastedt-Sieverstadt fault zone is located within the western branch of the Glückstadt graben.
Itzehoe fault
The 42 km long, NW-SE oriented Itzehoe fault belongs superordinately to the Glückstadt graben subdomain, and is located with the SE-part within the region of the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Block and with the NW-part within the western branch of the Glückstadt graben.
Allstedt-Altenbruch fault zone
The 47 km long, NNW-SSW/ NNW-SSE oriented Allstedt-Altenbruch fault zone belongs superordinately to the Glückstadt graben subdomain, and is located within the region of the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Block and partially runs within the south western Glückstadt graben.
Basdahl-Belmhusen fault zone
The 57 km long, N-S/NE-SW oriented Basdahl-Belmhusen fault zone is located within the region of the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Block and belongs superordinately to the Glückstadt graben subdomain.
We describe here the Southwestern Glückstadt Graben as a separate tectonostratigraphic block of the Glückstadt-Graben, whose boundaries are defined both by faults and salt walls as well as partly fuzzy trends in the lithofacies. Even though the main structures of this region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of the tectonic block and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the Southwestern Glückstadt Graben was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Outline definition: a) Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). b) Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. c) NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Uncertainties: Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. For References see also Tectonic boundaries in Germany.
Southwestern Glückstadt Graben
The subdomain of the southwestern Glückstadt graben represents a summary of southwestern parts, south of the ESE striking Neufeld Sand fault. the subdomain is also intersected by the ESE striking Wangerooge-Midlum fault. In this area, the Glückstadt graben trends S/SW into the Central North German Basin. [Domain type: Deformed sedimentary overburden, Basement: Avalonia.]
Cuxhaven-Büsum fault zone
The 54 km long, NNE-SSW oriented Cuxhaven-Büsum fault zone is located with the NW-part within the western branch of the Glückstadt graben and with the SW-part within the southwestern Glückstadt graben.
Wangerooge-Midlum fault
The 66 km long, WNW-ESE oriented Wangerooge-Midlum fault zone belongs superordinately to the Glückstadt graben subdomain, and is located within the region of the Southern Glückstadt Graben - Krummendeich - Hohenlockstedt Block and the Central North German basin.
Rüstringen fault zone
The 30 km long, NE-SW oriented Rüstringen fault zone belongs superordinately to the Glückstadt graben, and is located within the southwestern part therein.
Dedesdorf fault
The 30 km long, NNW-SSE oriented Dedesdorf fault belongs superordinately to the Glückstadt graben, and is located within the southwestern part therein.
Emtinghausen-Krautsand fault system
We describe the Emtinghausen-Krautsand fault system as a prominent narrow fault system which separates tectonic units in the centre of the northwestern part of the North German Basin and to the north seperates internal tectonic blocks of the Glückstadt Graben. Even though the main structures of this faulted region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this fault system was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
A N/NNE striking fault zone mostly with only minor offsets in base Zechstein (except in Glückstadt Graben). Characterized in the overburden by a chain of diapirs and salt walls with crestal structures. Crosses & bounds various parts of the NW part of the North German Basin - from the South Oldenburg Block to the southern Glückstadt Graben. The overriding fault pattern appears to be offset N-S along this zone, large-scale facies/strat. trends, on the other hand, seem to be only slightly influenced (e.g. Frisch & Kockel (2004). [Domain type: Strongly deformed sedimentary overburden, Basement: Avalonia.]
Emtinghausen-Krautsand lineament
We describe here the Mittelschleswig-Neumünster Block as a separate tectonic block of the Glückstadt-Graben, whose boundaries are defined both by faults and fault systems as well as salt walls. Even though the main structures of this region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of the tectonic block and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the Mittelschleswig-Neumünster Block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Outline definition: a) Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). b) Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. c) NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Uncertainties: Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. Uncertainties: 1.) Transition to CNGB is not clear in detail, 2.) Overburden structures are decoupled from the basement by halotectonics - thus overburden structures only approximately trace structures of the basement. For References see also Tectonic boundaries in Germany.
Mittelschleswig-Neumünster Block
The subdomain of the Mittelschleswig-Neumünster block represents the graben area east and north of the central area. Similar structural areas were grouped together. [Domain type: Deformed sedimentary overburden, Basement: Avalonia.]
Sterup fault
The 33 km long, N-S oriented Sterup fault is located within the Mittelschleswig-Neumünster block of the Glückstadt Graben subdomain.
Osterby-Schinkel fault
The 36 km long, NW-SE oriented Osterby-Schinkel fault is located within the Mittelschleswig-Neumünster block of the Glückstadt Graben subdomain.
Flensburg fault
The 40 km long, N-S oriented Flensburg fault is located within the Mittelschleswig-Neumünster block of the Glückstadt Graben subdomain.
Holnis fault
The 33 km long, N-S oriented Hölnis fault is located within the Mittelschleswig-Neumünster block of the Glückstadt Graben subdomain.
Mönkloh-Waabs fault zone
We describe here the Western branch Glückstadt Graben as a separate tectonostratigraphic block of the Glückstadt-Graben, whose boundaries are defined both by faults and salt walls as well as partly fuzzy trends in the lithofacies. Even though the main structures of this region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of the tectonic block and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the Western branch Glückstadt Graben was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Outline definition: a) Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). b) Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. c) NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Uncertainties: Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. For References see also Tectonic boundaries in Germany.
Western branch Glückstadt Graben
The subdomain of the western margin of the Glückstadt Graben represents a summary of western parts of the Glückstadt Graben. Several NNE striking salt walls in the overburden and underlying not always clearly defined basement faults. The domain is to the NW delineated from the West Schleswig Block by an ambiguous but steep slope (blind or previously unmapped basement fault). [Domain type: Deformed sedimentary overburden, Basement: Avalonia.]
Neufelder-Sand fault
The 54 km long, WNW-ESE oriented Neufelder-Sand fault is located within the western branch of the Glückstadt graben.
Oldenswort-Mildstedt fault zone
The 77 km long, NE-SW oriented Oldenswort-Mildstedt fault zone is located within the western branch of the Glückstadt graben.
Marne-Süderstapel fault zone
The 85 km long, NNE-SSW oriented Marne-Süderstapel fault zone is located within the western branch of the Glückstadt graben.
We describe here theCentral Glückstadt Graben as a separate tectonic block of the Glückstadt Graben, whose boundaries are defined both by faults and fault systems as well as salt walls. Even though the main structures of this basin have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of tectonic block and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the Central Glückstadt Graben was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Outline definition: a) Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). b) Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. c) NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Uncertainties: Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. For References see also Tectonic boundaries in Germany.
Central Glückstadt Graben
The subdomain of the Central Glückstadt graben represents the central part of the entire graben with the highest Triassic subsidence (reference e.g. Warsitzka et al. (2019), Baldschuhn et al. (1996, 1997)). [Domain type: Deformed sedimentary overburden, Basement: Avalonia.]
Oldenbüttel-Langsee fault zone
The 57 km long, NNE-SSW oriented Oldenbüttel-Langsee fault zone is located within the Central Glückstadt Graben.
Rendsburg fault zone
The 39 km long, W-E oriented Rendsburg fault zone belongs superordinately to the Glückstadt Graben subdomain and is located with the eastern part within the Central Glückstadt Graben, and with the western part within the western branch of the Glückstadt Graben.
Peissen-Westensee fault zone
The 42 km long, NNE-SSW oriented Peissen-Westensee fault zone is located within the Central Glückstadt graben.
Looft fault zone
The 34 km long, NW-SE oriented Looft fault zone is located within the Central Glückstadt Graben.
We describe here the eastern branch Glückstadt Graben as a separate tectonostratigraphic block of the Glückstadt-Graben, whose boundaries are defined both by faults and salt walls as well as partly fuzzy trends in the lithofacies. Even though the main structures of this region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of the tectonic block and the structures within has been made to date. The extent of this tectonostratigraphic sub-domain of the eastern branch Glückstadt Graben was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Redefined and summarized from Baldschuhn et al. (1996, 1997), Doornenbal & Stevenson (2010). Outline definition: a) Redefined and summarized from Baldschuhn et al. (1996) (especially structural maps and profiles), Baldschuhn et al. (1997), and the structure of the Base Zechstein based on the GTA & Doornenbal & Stevenson (2010). b) Especially related to the profiles of the GTA and observed major offsets in the base Z as well as high thicknesses of the Keuper, Buntsandstein. c) NNE striking salt walls of the region were taken into account as limiting structures of internal teconic units. Uncertainties: Depending on whether the contours are drawn based on the structure of the top basement or the distribution of sediments in the overburden, there may be major differences (salt tectonics/tectonic decoupling). The transition to the south into the Central Northwest German Basin cannot be clearly defined. For References see also Tectonic boundaries in Germany.
eastern branch Glückstadt Graben
Elmshorn-Sievershütten fault zone
The NE rim of the North German Basin subdomain roughly traces the NE rim of the NGB. Several units with a similar genesis were grouped together to a ESE striking sub-domain. The subdomain is characterized by a roughly south-dipping basin-slope and north-facing platform areas. A mostly concordant bedding of Mesozoic age smoothly transitions into shallow angular unconformities towards north. The subdomain include the Grimmen Wall, Rügen Depression and the Mecklenburg Bay. In addition, the east of this domain is characterized by SE to ESE running mainly normal faults of the the Vorpommern fault system. From the Grimmen High to the Agricola Fault System in the north, which is the border to the Arkona High, the domain is marked by a Jurassic rim basin of the North German basin, which is crossed by several SE striking faults. The most prominent of this fault zones/ grabens are the Werre & Prerow fault zones (Ahlrich et al. 2020). Uplift and moderate deformation characterize the subdomain during the Upper Cretaceous (uplift of the basin margins in the eastern part of the North German Basin) and the Jurassic basin of this area is inverted to a turtle-like structure. Domain type: Deformed sedimentary overburden, Basement: Avalonia/Baltica.
We describe the Northeastern rim of the North German Basin as a tectonostratigraphic unit along the norteastern rim of the North German Basin whose boundaries are not well defined. The outline is mainly derived from partly fuzzy trends in the lithofacies and local structural trends. Even though the main structures of this region have been described (e. g. Katzung & Ehmke, 1993), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalised for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future.
Northeastern rim of the North German Basin
The Vorpommeranian fault system - Grimmen Wall subdomain mainly shows SSE/SE striking faults between the Anklam fault in the S and the Bergen fault in the N. Most of the faults developed during the Triassic but also show partly Jurassic and Late Cretaceous activity.
We describe the Vorpommern fault system - Grimmen Wall as a tectonic sub-unit of the Northeastern rim region of the North German Basin. The outline is mainly derived from Mesozoic fault pattern (region with predominant SE/SSE striking fault zones). Even though the main structures of this region have been described (e. g. Krauss & Mayer, 2004), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Vorpommern fault system - Grimmen Wall
Vorpommern Fault System-Arkona High - Grimmen High
Samtens fault
The WNW-ESE running Samtens fault zone represents the northermost section of the supraregional Vorpommern fault system. The fault zone was formed during pre-Westfalian times and is characterized in the mesozoic overburden by an old-kimmerian, up to 6 km wide, alternating system of y-grabens.
Wiek fault system
The Wiek fault system defined by Seidel et al. (2018) represents a summary of the faults east of Rügen, crossing the Middle Rügen and Wolin blocks. The fault system consists of about 60 faults, flexures and other weakness zones. The fault system strikes from NW (Jasmund, Rügen) to SE until the Adler Kamien fault zone.
Samtens fault zone
The 31 km long, up to 6 km wide WNW-ESE running Samtens fault zone is located within the subdomain Northeastern rim of North German Basin. The fault zone is characterized by alternating Y-grabens preserving Jurassic and locally Lower-Cretaceous sediments. The fault zone also represents the northern part of the overregional Vorpommeranian Fault system.
Greifswald-Poseritz fault zone
The 34 km long, NNW-SSE oriented Greifswald-Poseritz fault zone is located in the NE rim of the North German Basin, and belongs to the eastern part of the Vorpommeranian fault system. The fault system is characterized by graben-like structures within the mesozoic overburden.
Reinberg fault zone
The 44 km long, NW-SE oriented Reinberg fault zone is located in the NE rim of the North German Basin, and belongs to the western part of the Vorpommern fault system. The fault system is characterized by grabenlike structures within the Mesozoic overburden.
Werre fault
17 km long, NNW-SSE oriented fault within the subdomain of Vorpommeranian Fault System - Grimmen Wall, located at the NE rim of the North German Basin.
Prerow fault
The 13 km long, W-E oriented Prerow fault is located at the NE rim of the North German basin and belongs to the Vorpommeranian fault system - Grimmen wall subdomain. Isolated remnants of Lower Cretaceous deposits (Wealden) with thicknesses inbetween 130 and 360 m occur.
Caledonian deformation front large-scale fault system
The Caledonian Deformation Front is characterized by a discordance, which represents the northernmost extension of the Caledonian accretionary wedge, located between over‐thrusting Ordovician sediments onto the southwestern margin of Baltica.
Agricola-Svedala fault
The Agricola‐Svedala Fault is located close to the Danish offshore region and shows an almost N‐S strike direction and dips steeply towards the west. According to Seidel (2019) the Cretaceous succession is especially affected by normal flexure causing an offset of about 25 ms.
Freest fault zone
NNW-SSE running fault zone within the Northeastern rim of the North German basin.
Wiek fault
The Wiek fault, located west of Rügen, is a prominent WNW-ESE running fault, which was formed during pre-Westfalian and reactivated in younger epochs. Fault throw are asssumed to be >3500 m, maximal values around 5 to 6 km. The fault is associated with a larger fault system, the Odense-Wiek fault system.
North Jasmund fault
The North Jasmund fault is a NW-SE running and southwest dipping, pre-Westfalian fault with throws of up to 3000 m. The fault is interpreted to be a part of the Wiek fault and the larger Odense-Wiek fault zone.
Adler-Kamien fault
Schaabe fault
The NW-SE running Schaabe fault was formed during the pre-Westfalian, dips northeast and is a normal fault.
Eastern rim of the North German Basin/ Szczecin-Kaliesz-East Brandenburg Swell
We describe the Eastern rim of the North German Basin/ Szczecin-Kaliesz-East Brandenburg Swell as a tectonostratigraphic unit along the western rim of the North German Basin, whose boundaries are not well defined. The outline is mainly derived from partly fuzzy trends in the lithofacies and local structural trends. Even though the main structures of this region have been described (e. g. Katzung & Ehmke, 1993), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
The subdomain of the eastern margin of the North German Basin represents a NNW striking structural unit and describes a roughly west-dipping basin slope. Mostly concordant bedding or shallow angular unconformities are found. To the west, the structural area is roughly separated from the Mecklenburg-Brandenburg depression by NNE to NNW striking basement faults. The region is characterized by enhanced Late-Triassic to Cretaceous stratigraphic hiatus. The northern boundary is roughly formed by the Anklam fault. Within this subdomain the eastern part of the NGB merges to the east into the Szczecin-Kaliesz-East Brandenburg Swell (Ostbrandenburg Schwelle), which delimits the NGB from the eastwardly adjoining Wolsztyn High and Mid-Polish Trough. [Domain type: Sedimentary overburden, Basement: Avalonia/Rhenohercynian/Saxothuringian.]
Usedom fault zone
The 35 km long and NNW-SSE running Usedom fault zone is located within the subdomain Eastern rim of North German basin. The fault zone is characterized by a graben with a major normal fault at the eastern flank.
Buckow fault
The NNE-SSW striking Buckow fault is located southeast of the Mecklenburg-Brandenburg depression, and is often interpreted as the eastern part or eastern extension of the Potsdam fault. The Buckow fault crosses as reverse fault the Buckow salt pillows Buckow and Bad Freienwalde.
Möckow-Dargibell fault zone
The 50 km long, 5 km wide and NNW-SSE running Möckow-Dargibell fault zone is located within the subdomain Eastern rim of North German basin. The fault zone is characterized by a graben, with a major normal fault at the eastern flank and belongs to the Vorpommern Fault system.
Thrusted Central North German Basin sub-domains
We describe the thrusted Central North German Basin sub-domains as a summary of separate tectonic units, which show great similarities in the type of deformation, their basin location and the orientation of faults and salt structures. The outline of the summarized units are predominantly defined both faults and fault systems. Areas of significant Upper Cretaceous contractional deformation of the Mesozoic overburden within the Central North German Basin were summarized to specific tectonic units. Even though the main structures of this regions have been described partly in detail (e. g. Baldschuhn et al., 2001), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain border and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Based on a compilation of Baldschuhn et al. (1996, 1997), Röllig et al. (1990). Outline definition/ existing outlines based after fault and deformation pattern (Late Cretaceous deformationa) in the Mesozoic overburden; considering of strike-domain pattern and orientation of the salt structures. Designation is based on overview maps and assumed outcrop geometries in the case of Röllig et al. (1990). The structural subdomains are not bounded at all their boundaries by discrete faults, but also by outcrop patterns of stratigraphies. For References see also Tectonic boundaries in Germany.
The subdomains of the thrusted Central North German basin are a summary of a total of four structural regions separated from each other, which in turn are subdivided by further blocks in the literature. However, these regions show great similarities in the type of deformation, their basin location, orientation of faults and salt structures. These structural domains fringe/adhere to the north of strongly inverted areas or areas uplifted during the Upper Cretaceous. However, these regions as a whole are assigned to the central area of the NGB in subsidence history & corresponding to facies and lithostratigraphy (central basin location/relatively submerged). The structural domains are characterized by a dominance of ESE to SE striking faults, often associated with salt structures elongated in the same direction in the Mesozoic overburden. Partially, areas are also assigned in former literature to the Pompeckj Block region. Among others, Müller et al. (2016) discussed the non-conforming subdivision and designation of the Pompeckj Block. Irrespective of the partly strong structuring of the Mesozoic overburden of these regions, the base Zechstein often shows only minor vertical offsets.
Rotenburg-Soltau-Eldingen Block
We describe the Rotenburg-Soltau-Eldingen Block as a seperate tectonic unit of the sub-domain thrusted Central North German Basin. The outline of this tectonic unit is predominantly defined by Mesozoic, esp. Late Cretacous structural pattern. Neighbouring areas of significant Upper Cretaceous contractional deformation of the Mesozoic overburden within the Central North German Basin were summarized to this specific tectonic unit. Even though the main structures of this regions have been described partly in detail, no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. New defined and summarized from Baldschuhn et al. (1996); especially from structural maps and profiles), Baldschuhn et al. (1997), as well as the structure of Base Zechstein. Definition of outline mainly oriented to Baldschuhn et al. (1997). Uncertainties: Different definitions in dependence to different interpretation of structural pattern in the overburden and basement. For References see also Tectonic boundaries in Germany.
The subdomain of the Rotenburg-Soltau-Eldingen block is located in the area of moderate to minor Upper Cretaceous contraction north of the Allertal fault system. After Baldschuhn et al. (1997) this region is subdivided into a number of individual basement blocks (Rotenburg/Schneverdingen/Soltau/Munster/Schmarbeck/Bahnsen/Eldingen/Wesendorf). This pattern also coincides in large parts with the pattern of the Mesozoic overburden. The lithostratigraphic sequence of this region follows in large parts the pattern described as the Pompeckj Block. In the west the subdomain is bounded by the Emtinghausen-Krautsand lineament and to the east by the Braunschweig-Gifhorn fault zone. An important lineament in the north of the unit is formed by the Uelzen lineament. Domain type: Deformed sedimentary overburden, Basement: Avalonia/Rhenohercynian(?).
Scheessel-Fallingbostel fault zone
The 42 km long, NNW-SSE running Scheesel-Fallingbostel fault zone is located in the central part of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. In the northern part normal faults dominate the kinematics.
Süstedt-Bahnsen-Fassberg fault zone
The 23 km long, WSW-ENE running Südstedt-Bahnsen-Fassberg fault zone is located in the central part of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. The fault zone is characterzied by the associated salt structures Bahnsen and Niendorf II, the inversion structure Fassberg and the graben Bahnsen.
Volkwardingen fault
The 62 km long, W-E running and S-dipping Volkwardingen basement fault is located at the northern rim of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. With this fault the salt structures Scheessel, Stemmen, Otter-Todtshorn and Volkwardingen are associated.
Taaken fault
The 37 km long, W-E running and S-dipping Taaken basement fault is located at the northern rim of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. With this fault the salt structures Taaken, Scheessel and Ostervesede are associated.
Wardböhmen fault
The 9 km long, WSW-ENE running Wardböhmen normal fault is located close to the SW-border of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. Associated with this fault is the salt structure Wardböhmen (Frisch & Kockel 2004).
Lüdingen fault
The 19 km long, NNE-SSW running Lüdingen normal fault is located at the SW-border of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. In the southern part the fault is located within the Allertal fault system. Associated with this fault is the salt structure Lüdingen.
Böstlingen-Unterlüß fault zone
The 62 km long, W-E running Böstlingen-Unterlüss fault zone is located in the southern part of the Rotenburg-Soltau-Eldingen block and belongs to the thrusted part of the Central North German basin. This fault zone is associated with inversion and salt structures and is predefined by basement faults, which show Lower Permian synsedimentary activity.
We describe the East-Brandenburg - North Sudetes Depression as a separate tectonic unit of the subdomain thrusted Central North German Basin. The outline of this tectonic unit is predominantly defined by distributional/erosional pattern and prominent faults. Neighbouring areas of significant Upper Cretaceous contractional deformation of the Mesozoic overburden within the Central North German Basin were summarized to this specific tectonic unit. Even though the main structures of this regions have been described partly in detail, no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: Voigt (2009), Röllig et al. (1990). Outline definition: The outline based on the outcrop of Upper Cretaceous sediments after Röllig et al. (1990) and encloses the major SE-striking structural features of the region. The NW boundary was drawn at the Rüdersdorfer Salzkisssen, although no clear boundary to northwest-adjacent basin parts is evident. The envelope includes basin areas with clear Upper Cretaceous overprint. Uncertainties: (a) boundary to the NW to the tectonostratigraphic domain Central North German Basin not unambiguous; (b) boundary to the structure of the Prignitz-Lausitz Wall not to be unambiguously fixed to structures - from there fixed by the outline of the Upper Cretaceous. Existing outlines: Depicted in Voigt (2009), among others. This outline presented here oriented on structures did not exist in this form so far. For References see also Tectonic boundaries in Germany.
East-Brandenburg - North Sudetes Depression
The East Brandenburg-North Sudetes depression subdomain is an Upper Cretaceous foreland basin located between the uplifts of the Lusatian-Riesengebirge anticlinal zone and the North Sudetes anticlinal zone. The structural domain is traversed by partly complex SE-striking inverted graben zones/fault zones. The best known of these is the Fürstenwalde-Guben fault zone. In general, it is an area of minor to moderate shortening during the Upper Cretaceous. Beutler & Stackebrandt (2012) subdivide the domain into the Mittenwald & Guben Block. [Domain type: Late Cretaceous sedimentary basin; Basement: Rhenohercynian/Saxothuringian]
Fürstenwalde-Gubener fault zone
The Fürstenwalde-Guben fault zone is a NW-SE to NNW-SSE dipping wide fault zone in the East Brandenburg-North Sudetes depression within the thrusted Central North German basin. The fault zone is characterized by anticlines with horst-like and locally intrasalinar-tectonic structures.
Rüdersdorf fault
The Rüdersdorf fault is located in the East Brandenburg-North Sudetes depression within the thrusted Central North German basin, extends over 32 km, runs WSW-ENE and is associated with the Rüdersdorf salt pillow.
We describe the Altmark Fläming Depression as a seperate tectonic unit of the subdomain thrusted Central North German Basin. The outline of this tectonic unit is predominantly defined both by faults and fault systems. Neighbouring areas of significant Upper Cretaceous contractional deformation of the Mesozoic overburden within the Central North German Basin were summarized to this specific tectonic unit. Even though the main structures of this regions have been described partly in detail, no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Saxony-Anhalt provides and describes a partly more detailed and updated fault data set of Saxony-Anhalt within the framework of the HIKE project (DE-ST-0, DE-ST-1000). Outline definition based on outcrops of the Mesozoic at the base Tertiary esp. from Röllig et al. (1990) & Martiklos et al. (2001). Also referring to Baldschuhn et al. (1996). Uncertainties: a) diffuse transition to the Prignitz Wall and the northward following central less deformed basin parts b) overthrusted from the south - thus in detail overlapping of the outlined blocks c) slightly different boundary drawing depending on which outcrop at the base Cenozoic in the overburden is followed if not explicitly a fault is shown as boundary. In this case the outline of the Upper Cretaceous was followed. As a region in a lot of the literature designated among others Katzung & Ehmke (1993), but never discretely outlined until now.
Altmark Fläming Depression
The subdomain of the Altmark-Fläming Depression represents the area north of the basement uplifts of Gardelegen & the Upper Cretaceous uplifted Halle-Wittenberg Block in the south and the inverted basin areas in the strike of the structural unit Prignitz - Lausitz - Riesengebirge Anticlinal Zone (in this area Prignitz wall). Bounded to the west by the NNE/N trending Brunswick-Gifhorn-Lüneburg fault system. Especially the western parts of the structural unit are influenced by movements along the Eichsfeld-Altmark sill (esp. in the Buntsandstein, Rotliegend, Keuper). The overburden is characterized by several SE-striking syncline-anticline structures caused by foreland thrusting of the Gardelegen thrust (e.g. Jähne & Kley, 2008). Thick synkinematic Upper Cretaceous is deposited in the synclines. The anticlinal structures coincide with salt structure lineaments. In contrast, the base Zechstein shows only minor offsets. Further REF: Jähne & Kley (2008), Benox et al. (1997), Otto (2003), Malz et al. (2020). Map Reference: Based on compilation of Baldschuhn et al. (1996) (overburden structures) and Martiklos et al. (2001), Röllig et al. (1990).[Domain type: Deformed sedimentary overburden; Basement: Avalonia]
Altmersleben-Demker zone
The Altermersleben-Demker structural zone is located within the Altmark-Fläming depression of the thrusted Central North German basin, extends over a length of 29 km and is oriented NW-SE.
Ahlum fault
The 11 km long, WNW-ESE running Ahlum fault is a asymmetric and compressive overprinted and salt core containing fault.
Apenburg-Wernstedt fault
The NW-SE running Apenburg-Wernstedt fault is located within the centre of the Altmark-Fläming depression and extends over 37 km.
Rosenthal-Gülden-Peckensen fault zone
The 23 km long, N-S running fault system is located at the eastern rim of the eastern part of the Lower Saxony Basin, and runs almost parallel to the Braunschweig-Gifhorn fault system.
Rosenthal-Gülden-Braudel-Peckensen fault zone
The N-S running Rosenthal-Gülden-Braudel-Peckensen fault zone extends over 103 km, representing at the southern tip the border between the Gardelegen-Rosslau uplift and the Braunschweig-Gifhorn-Lüneburg fault system, in the middle section representing the border between the Braunschweig-Gifhorn-Lüneburg fault system and the Altmark-Fläming depression and at the northern part the border between the Braunschweig-Gifhorn-Lüneburg fault system and the Central North German basin.
Liebenwalde fault
The 7 km long, NNE-SSW running Liebenwalde fault represents the southwestern section of the Liebenwalde-Torgelow fault. The Liebenwalde fault is located within the SE area of the Altmark-Fläming depression of the thrusted Central North German basin.
Gardelegen fault
The 153 km long, WNW-ESE running Gardelegen fault is located at the southern boundary of the Altmark Fläming depression within the thrusted part of the Central North German basin. The fault represents a listric, SW-dipping steep reverse fault that was formed in the course of Upper Cretaceous inversion. Due to seismic data, the fault reaches a depth of up to 25 km.
Genthin fault
The 90 km long, WNW-ESE running Genthin fault represents a listric, SW-dipping reverse fault, that was reactivated in the course of Upper Cretaceous inversion.
Südoldenburg & Hoya Block
We describe the Südoldenburg & Hoya Block as a seperate tectonic unit of the subdomain thrusted Central North German Basin. The outline of this tectonic unit is predominantly defined by Mesozoic, esp. Late Cretacous structural pattern. Neighbouring areas of significant Upper Cretaceous contractional deformation of the Mesozoic overburden within the Central North German Basin were summarized to this specific tectonic unit. Even though the main structures of this regions have been described partly in detail, no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map reference: Based on a compilation by Baldschuhn et al. (1996, 1997). Outline of structure is based on Mesozoic structures as defined by Baldschuhn et al. (1996). Uncertainties: (a) diffuse transition in the area of the Hoya Block towards the Lower Saxony Basin and its sub-units; (b) partly overlain in the south by the inverted LSB - thus actually an overlap of structural areas; (c) slightly different boundary drawing depending on designation according to basement or overburden structure; (d) whether areas further west were also shortened by the Upper Cretaceous and show similar deformation is difficult to prove at present. If so then the boundary could also coincide with the Ems lineament. Currently this structural area borders the unit East Frisia - Ems Estuary Region. For References see also Tectonic boundaries in Germany.
The subdomain of the Südoldenburg & Hoya block is located north of the Lower Saxony Basin. In the south it is bounded by the partially overlapping structural features Rheder Moor - Oythe & Goldenstedt - Blenhorst and in the north by the less constricted Leer-Bremen lineament. To the north of the LSB, an Upper Cretaceous foreland basin has developed on the Ostfriesland Block. To the east, the subdomain is separated from the NE Lower Saxony Basin by the Emtinghausen-Krautsand fault zone. To the west, the boundary roughly coincides with the overturning Jemgum structure and associated Jemgum fault. Domain type: Deformed sedimentary overburden, Basement: Avalonia.
Leer-Bremen fault zone
The 130 km long, NW-SE/WNW-ESE running Leer-Bremen fault zone is located in the Südoldenburg-Hoya block and belongs to the thrusted part of the Central North German basin, to which several inversion structures are associated.
Vegesack-Lilienthal fault zone
The 55 km long, WNW-ESE running Vegesack-Lilienthal fault zone is located in the Südoldenburg-Hoya block and belongs to the thrusted part of the Central North German basin. Associated with this fault zone are the inversion structure Bremen, salt structure Lilienthal, inversion structure Wührden, salt structure Lesum and inversion structure Vegesack.
Jemgum fault
The 34 km long, NNE-SSW running Jemgum fault is located in the Südoldenburg-Hoya block and belongs to the thrusted part of the Central North German basin.
Braunschweig-Gifhorn-Lüneburg fault system
The Lutter-Salzgitter fault zone is a 14 km long fault zone in the southern extension of the Braunschweig-Gifhorn-Lüneburg fault system and with a NNE-strike. This fault zone crosses the Subhercynian Cretaceous Basin and transfers offsets to the adjacent Harz fault system to the south.
Lower Saxony Basin
The Lower Saxony Basin is located in the southwest of the North German basin (NGB), which is itself a segment of the NGB. Including its uplifted parts the LSB is approx. 250 km long in a NW-SE direction and from 60 km to more than 100 km wide. Its structural and sedimentary evolution diverges from the rest of the NGB in Late Jurassic to Early Cretaceous time. Besides increased subsidence of the entire LSB, several mostly ESE to SE trending grabens and half-grabens evolved and are connected by major fault systems which enclose most of the basin (e.g. Allertal Lineament). The central part of the LSB (Central Lower Saxony Basin subdomain) shows little Late Jurassic to Early Cretaceous faulting. Late Cretaceous contraction of the LSB takes different forms in the Mesozoic basin fill, but NNE/NE dip-slip contraction is suggested by the majority of structures such as: a) A broad anticlinal inversion of the entire basin, with maximum uplift over the former centre of the LSB, b) Major reactivation and inversion of grabens and faults along the borders of the LSB. Often entire grabens are upwarped while normal offsets on faults are preserved, c) Broad regional uplift in the hanging wall of the Osning Thrust, d) Bulging of formerly flat-lying Upper Jurassic or Lower Cretaceous sub-basin fills, e) Compressional overprinting of different forms of salt diapirs, f) Formation of compressional salt-anticlines, g) Subordinate formation of new thrust and reverse faults, h) Indications for strike-slip faulting and strain partitioning along unfavourably oriented NNE striking lineaments (e.g. Gifhorn-Braunschweig fault zone) but no clear evidence for NE/NNE dip-slip contraction. Up to 7 kilometres of Triassic to Upper Cretaceous sedimentary strata may have been eroded along the southern rim of the Central Lower Saxony subdomain. The uplift is related to the reactivation and inversion of the southern border fault system (Osning Lineament) of the LSB, but the strong erosion of its hanging-wall makes it difficult to quantify the contraction from structural data. The Lower Saxony Basin is bordered to the south by the Osning lineament and the Münsterland Cretaceous Basin, and to the north by the Aller lineament (Adriasola Muñoz (2007), Baldschuhn & Kockel (1999), Lohr 2007). Several fault zones in-between run from NW to SE, but to the east and west, this basin is again limited by structural lineaments running from N to NNE (e.g. Ems lineament, Braunschweig-Gifhorn fault zone). [text mainly taken from Jähne-Klingberg et al. (2016)]
NE Lower Saxony Basin
NE-part of the Lower Saxony Basin. This part of the basin is bounded NE by the Allertal fault system, east by the Braunschweig-Gifhorn fault system, SE by the Steinhuder Meer - Stemmer Berg - Limberg fault system. As the Central Lower Saxony basin towards SW, this basin part shows also a broad anticlinal basin inversion but in a more moderate style. [Domain type: deformed sedimentary overburden, Basement: Rhenohercynian/Avalonia.]
We describe the Northeastern Lower Saxony Basin as a tectonostratigraphic unit, whose boundaries are defined both by faults and fault systems as well as partly fuzzy trends in the lithofacies. Even though the main structures of this region have been described in detail (e. g. Baldschuhn et al., 2001), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Marienburg-Wienhausen fault zone
The 57 km long, NE-SW running Marienburg-Wienhausen fault zone is located within the NE-Lower Saxony Basin at the northern tip within the Allertal fault system. Along this basement fault zone, salt diapirs and inverted grabens are associated in the overburden (Baldschuhn & Kockel 1998).
Linsburg fault
Lauenau-Bad Münder fault
The Lauenau-Bad Münder fault is a 33 km long, WNW-ESE striking normal fault in the eastern extension to the Petershagen fault (DE-817). Associated with this fault is a halfgraben at Bad Münder.
Allertal fault system
The Lower Saxony Basin is bounded to northeast by a complex lineament consisting of shortened diapirs and inverted grabens (Allertal Lineament). It is a several kilometer broad and an intensely structured zone, which can be subdivided into several inverted and shortened structures, with mostly ESE/SE strike in the Mesozoic overburden. However, the base Zechstein shows only little relief. The geometry of the salt structures along the lineament is highly variable with occurrence of lateral salt intrusions into Mesozoic salt formations and salt-filled fault zones. [Domain type: strongly deformed overburden, Basement: Avalonia/Rhenohercynian(?)]
We describe the Allertal fault system as a sub-region of the Northeastern Lower Saxony Basin which is highly dissected by several major sub-parallel fault zones with a mostly similar development history. Even though the main structures of this region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this faulted block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Wietze graben fault system
The 8 km long, NE-SE running Wietze graben fault system is located within the Allertal fault system. The graben is characterized by two SE-dipping normal faults and an antithetic SE-dipping normal fault causing a Y-graben, reaching up to the Lower Cretacous (Barreme). Movements along the SE-dipping major faults are documented for Keuper and Lower/Midlle Jurassic times, inversion during Coniac-Santon results in the uplift of of the southeastern flank.
Bassen-Celle fault zone
The Bassen-Celle fault zone extends over 121 km length and belongs genetically to the Allertal fault zone. As main structural elements of the Bassen-Celle fault zone graben in the basement and horsts are documented for Buntsandstein times. Several times active since Lower Bunter times, this fault zone represents as normal fault the northern rim of the Lower Saxony basin since the Middle Jurassic, especially within the Upper Jurassic and Lower Cretaceous. This structure was compressively overprinted and partly inverted during the Upper Cretaceous.
Martfeld-Hope fault zone
The 60 km long, WNW-ESE oriented Martfeld-Hope fault zone is located at the southwestern border of the Allertal fault system. This structure was compressively overprinted and partly inverted during the Upper Cretaceous.
Verden-Wietze fault zone
The NW-SE running Verden-Wietze fault zone is located within the central part of the Alltertal fault system, is 78 km long and since the Triassic was (re)activated several times, sometimes as NE-normal fault, sometimes as SW-normal fault. Subsequently, this structure was strongly compressively overprinted during the Upper Cretaceous.
Mölme-Stederdorf-Plockhorst fault zone
This 40 km long, NNE-SSW running fault zone is associated with two graben structures, the Stederdorf graben and the Plockhorst graben as well as two salt structures. The fault zone is located in the eastern part of the Lower Saxony Basin and separates the Hildesheim Block in a western and eastern part.
SE Lower Saxony Basin
This structural domain is a less deformed and less inverted basin part of the Lower Saxony Basin southwest of the Steinhuder Meer - Stemmer Berg - Limberg fault system. [Main Strike: ESE/SE, Domain type: Sedimentary overburden, Basement: Rhenohercynian.]
We describe the Southeastern Lower Saxony Basin as a tectonostratigraphic unit, whose boundaries are defined both by faults and fault systems as well as partly fuzzy trends in the lithofacies. Even though the main structures of this region have been described in detail (e. g. Baldschuhn et al., 2001), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Lübbecke fault
The Lübbecke fault has a length of 20 km, runs from northeast to southwest and connects the Petershagen fault with the Wiehengebirgs fault.
Brünninghausen-Leinetal fault zone
Hameln-Elfas-Salzderhelden fault system
The NW-SE oriented Hameln-Elfas-Salzderhelden fault zone represents one segment of the southern border of the Lower Saxony Basin east of the Weser river. This fault zone separates the Solling block in NE from the Hils block. Most important element of this fault zone is the Elfas thrust, active in the Upper Cretaceous.
Osning-Wiehengebirge thrust unit/ uplift
Uplifted part of the Southern Lower Saxony Basin in the hanging wall of the north east dipping Osning fault. The inversion of the Lower Saxony Basin reaches up to 7 km. The Osning thrust borders the domain in the south to the Münsterland Basin, which does not belong to the North German Basin. [Domain type: Basement uplifts under coverage, Basement: Rhenohercynian/Avalonia]
We describe the Osning-Wiehengebirge thrust unit/ uplift as an uplifted strongly faulted sub-unit of the western Lower Saxony Basin in the west of the Ems Lineament. Even though the main structures of this faulted region have been described in detail (e.g. Baldschuhn & Kockel, 1999, Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this faulted block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Wiehengebirgs-Wesergebirgs fault zone
The 42 km long Wiehengebirge-Weser fault system is part of a wide partly broken flexure along the northern border of the Osning Wiehengebirge thrust unit of the Lower Saxony Basin. This fault system also is associated to the Wiehengebirgs fault system further west (DE-814).
Wiehengebirge fault zone
The 35 km long Wiehengebirge fault system is part of a wide partly broken flexure along the northern border of the Osning Wiehengebirge thrust unit of the Lower Saxony Basin. This fault system also is associated to the Wiehengebirgs-Wesergebirgs fault system (DE-823). This flexure merges into the Lübbecke and Neuenkirchen fault zones and is presumably the result of a blind thrust zone.
Neukirchen fault
The Neuenkirch fault is a 39 km long, NW-SE running reverse fault partly belonging to Osning Wiehengebirge thrust unit of the Lower Saxony Basin and partly to the North Westphalia Lippe subfault system, and borders the Neuenkirchen Block.
Neuenkirchen fault
Suttrup-Schapen fault
The NNW-SSE running Suttrup-Schapen fault is located in Osning Wiehengebirge thrust unit of the Lower Saxony Basin east of the Ems lineament, and is 32 km long.
Bad Meinberg-Egge fault zone
The N-S running Bad Meinberg-Egge fault zone is a complex fault zone of 65 km length, that separates the North Westfalia subfault system and the Westfalien bight subdomain in the west to the Pyrmont and Solling Block in the East. Eastern border of the Osning Wiehengebirge thrust unit. During Late Cretaceous transpressiv/ dextral movement.
Osning fault system
Prominent fault system located at the southern rim of the Lower saxony Basin, creates locally as much as 7 km vertical offset. Due to structural inversion during the Upper Cretaceous and associated deep erosion, these high vertical offsets are not obvious in the today’s geological maps. WNW-ESE running faults of a length of 43 and 53 km respectively.
Western Lower Saxony Basin
Basin parts of the LSB west of the Ems-Linemaent. [Domain type: deformed overburden, Basement: Avalonia]
We describe the western Lower Saxony Basin as a tectonostratigraphic unit, whose boundaries are defined both by faults and fault systems as well as partly fuzzy trends in the lithofacies. Even though the main structures of this region have been described in detail (e.g. Baldschuhn & Kockel, 1999, Baldschuhn et al., 2001), no clear definition of the outline of this basin part has been made to date. The extent of this tectonostratigraphic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Neuringe-Osterbrock fault
The Schale fault is an 18 km long, NNW-SSE running reverse fault in the western part of the Lower Saxony Basin.
Neuringe Osterbrock fault
Laar-Völzel fault
Ratzel fault
Gronau-Waldhügel-Nordhorn thrust unit/ uplift
During the Late Cretacous strongly uplifted marginal area of the Western Lower Saxony Basin similar to Osning Wiehengebirge thrust unit. The most prominent structures are the inverted Gronau - Waldhügel fault zone/graben and the Nordhorn fault.
We describe the Gronau-Waldhügel-Nordhorn thrust unit/ uplift as an uplifted strongly faulted sub-unit of the western Lower Saxony Basin in the west of the Ems Lineament. Even though the main structures of this faulted region have been described in detail (e.g. Baldschuhn & Kockel, 1999, Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this faulted block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Neuenhaus fault
Balderhaar fault
The Balderhaar fault is located within the Balderhaar Block, is 19 km long and oriented NW-SE.
Reutum fault
Gronau-Waldhügel fault zone
Gronau Waldhügel fault zone
The 44 km long, W-E running Gronau-Waldhügel fault zone represents the western extension of the Osning fault system. The fault zone borders the SSW-rim of the Lower Saxony Basin against the Westfalian Bight.
Schuttorf graben fault system
The Schuttorf fault system is a N-S /NNW-SSE running graben system, is located in southern extension of the Ems Graben and belongs to the Schuttorf Block. It extends from 17 (DE-815) to 29 km (DE-821) respectively.
Emelichheim-Schoonebeck fault
Esche-Laar fault
The Esche-Laar fault is 14 km long and runs NNW-SSE within the Western part of the Lower Saxony Basin.
Steinhuder Meer-Stemmer Berg-Limberg fault system
We describe the Steinhuder Meer-Stemmer Berg-Limberg fault system as a prominent narrow fault system which separates the Northeastern Lower Saxony Basin from the Central Lower Saxony Basin and the Southeastern Lower Saxony Basin. Even though the main structures of this faulted region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this faulted block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
The NNE-SSW running, 56 km long Steinuder Meer-Stemmer Berg-Limberg fault system is located at the border between the Central and Eastern part of the Lower Saxony Basin. [Domain type: Strongly deformed sedimentary overburden, inverted structure (Late Cretaceous), partly prominent thrusts Basement: Rhenohercynian/Avalonia.]
Dipping Harz structure & Sack depression
Dipping of the Harz anticline below thick Mesozoic overburden. The Mesozoic overburden is characterized by thrusts, which borders synclines with Jurassic to Cretaceous outcrops. It is a marginal part of the Lower Saxon Basin but strongly influenced by NNE striking elements aligned along the Eichsfeld-Altmark swell. [Outcrop age: Triassic, Cretaceous; Domain type: Basement uplifts under coverage, Basement: Rhenohercynian.]
We describe the dipping Harz structure & the Sack depression as a tectonic sub-unit of the Lower Saxony Basin whose boundaries are defined both by faults and fault systems as well as by the structure of the Pre-Zechstein. Even though the main structures of this region have been described in detail (e. g. Baldschuhn et al., 2001), no clear definition of the outline of this basin part has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Waddekath Bonese fault zone
The Rosenthal-Gülden-Braudel-Peckensen fault zone predominantly is located within the northern Eichsmark-Altmark Swell, while the southern tip is associated with the Braunschweig Gifhorn fault system. The southern extension is formed by the Weddingen-Nettgau fault zone (DE-884).
Horndorf Rosche Thondorf fault zone
55 km long, NNE-SSW running fault within the Braunschweig-Gifhorn-Lüneburg fault system.
Southern Ems fault system
Schale fault
The NNW-SSE running Ems fault system is located in southern extension of the Ems graben structure, has a length of 16 km and represents the border between the western and central part of the Lower Saxony Basin. The lineament is not affected by strike-slip movements of the crossing Osning lineament (Baldschuhn & Kockel 1999)
Southern Ems fault
The Lohne-Pollersand fault is a 43 km long, NW-SE running fault within the central part of the Lower Saxony Basin and runs almost parallel to the Ems lineament in the west and to the Schale Störung in the east.
Lohne Pollersand fault
Weddingen-Nettgau fault zone
The 64 km long, NNE-SSW running Broistedt-Wittingen fault zone is located at the W-border of the Braunschweig-Gifhorn-Lüneburg fault system and borders in the northern part to the Allertal fault system. The fault zone was involved in the sedimentary and structural development of the Eichsfeld Altmark Swell.
Ems fault system
Flachstöckheim-Immendorf fault zone
The NNW-SSE running Bechtsbüttel-Vordorf fault zone is located within the eastern part of the Lower Saxony Basin, has a length of 20 km and is located close to the Braunschweig-Gifhorn fault zone. The fault zone is associated with the salt diapir Bechtbüttel.
Ems graben fault system
We describe the Ems Lineament as a prominent strongly faulted unit with grabens and mostly subparallel fault-zones (generalized interpreted as fault system), which crosses or borders several structural units of the North German Basin. Even though the main structures of this faulted region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this faulted block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
The Ems fault system is a 140 km long, NNW-SSE running system of mainly SSE striking grabens and fault zones. It crosses the Lower Saxony Basin in the East. Many of the WNW-ESE fault zones of the central part of the Lower Saxony Basin end or lose significant offset in the Ems lineament area. The Ems Lineament can be broadly regarded as the western boundary of the North German Basin and thus represents the transition to the Anglo-Dutch Basin. The Ems lineament is the southern part of a larger system of predominantly SSE striking elements that can be traced into the Horn Graben. Rifting of the Ems graben within the Lower Saxony Basin started in Lower Gipskeuper times, continued until Upper Gipskeuper times and was followed by inversion in Late Cretaceous (Kockel 2002). [Domain type: Strongly deformed overburden, basement: Avalonia]
Broidstedt-Wittingen fault zone
The Braunschweig-Gifhorn fault system represents the eastern border of the Lower Saxony Basin and consists of several segments, predominantly oriented N/NNE-S/SSW and subordinate NE-SE and NW-SE respectively. During Early to Middle Buntsandstein time an early stage of reactive salt diapirism takes place followed by sub-salt normal faulting and reactive diapirism in the Late Buntsandstein to Muschelkalk in this fault zone (Warsitzka et al. 2018).
Bechtsbüttel-Vordorf fault zone
We describe the Braunschweig-Gifhorn-Lüneburg fault system as a prominent strongly faulted unit with mostly subparallel fault zones (generalized interpreted as fault system), which crosses or borders several structural units of the North German Basin. The structural unit defined here is a generalization of contiguous fault systems. Even though the main structures of this faulted region have been described in detail (e.g. Baldschuhn et al., 2001), no clear definition of the outline of this strongly deformed block has been made to date. The extent of this faulted block was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Mainly NNE striking faults. Most of the Mesozoic this structural element show predominantly extensional tectonics (mainly westward dipping, salt influenced extensional structures) but also a strike-slip component can be assumed (especially during the Permian and Late Cretaceous). [tectonic style: halo-tectonics, extensional tectonics, partly strike-slip tectonics; Domain: Stronlgy deformed overburden, Basement: Rhenohercynian/ Avalonia(?)]
Braunschweig-Gifhorn fault zone
The 44 km long Gronau-Waldhügel fault zone represents the southern border of the Lower Saxony Basin. It crosses the Ems fault system domain without major strike-slip offset.
Rühle fault
E-W striking fault crossing the Ems fault system.
Lutter-Salzgitter fault zone
Central Lower Saxony Basin
Jurassic to Wealden basin center. The whole Central Lower Saxony Basin was inverted during the Late Cretaceous as a broad anticlinal uplift. Most of the faults run along the northern and southern edges of the structural domain. [type: deformed sedimentary overburden, Basement: Avalonia.]
Petershagen fault
The Petershagen fault represents the southern graben fault of the WNW-ESE running Rehburg graben, is located within the central part of the Lower Saxony Basin and extends over a length of 59 km.
Bad Nenndorf fault system
The Bad Nenndorf fault system is a 13 km long, ENE-WSE running graben. The graben was initiated within the Middle Jurassic, was intensified within the Lower Cretaceous and lasted until Aptian times. No indications are found for inversion of the graben during Coniac - Santonian times.
Rehburg fault system
The Rehburg fault system is a WNW-ESE running graben structure of 53 km length and 14 km width. The northern border of this graben is the southward dipping and listric Rehburg fault, the southern border the northward dipping Petershagen fault.
Central Lower Saxony Basin fault system
The Anticlinal uplift of the Central Lower Saxony Basin is bounded to the north by several ESE/SE striking faults. These faults show both normal and reverse components and are often part of inverted graben structures.
Deblinghausen fault
A 37 km long, W-E running fault within the Lower Saxony Basin.
Voigtei fault
The Voigtei fault borders the Voigtei block, extends over 34 km, strikes W-E and almost parallel to the Rheder Moor Oythe fault zone further North. The fault is located in the central part of the Lower Saxony Basin.
Hemmelte-Bokern fault
The Hemmelte-Bokern fault extends over 48 km, strikes WNW-ESE and is located at the northern rim within the central part of the Lower Saxony Basin.
Addrup fault
Goldenhorst-Blenhorst fault zone
A 72 km long and W-E striking fault zone and along the northern rim of the Lower Saxony basin.
Rheder-Moor-Oythe fault zone
A 140 km long and WNW-ESE striking fault zone, representing the northern rim of the Lower Saxony basin.
Aschen fault
A 90 km long, WNE-ESE striking fault in elgongation to Neufeld-Rehburg fault.
Rehden fault
Neufeld Rehburg fault
A 56 km long, WNW-ESE running normal fault in the central part of the Lower Saxony Basin. The fault represents the northern flank of the Rehburg Graben.
Oberlanger Tenge - Löningen fault zone
A 125 km long lineament, with WNW-ESE strike in the north of the Osning lineament.
Kalkriese-Hunteburg fault
The Kalkriese-Hunteburg fault runs W-E, extends over 44 km and is located close to the transition from the Central Lower Saxony Basin to the North Westphalia Lippe Subfault system.
Ems Lineament
We describe the Teisseyre-Tornquist zone (TTZ) as a tectonic unit, whose boundaries are mainly defined by faults and the extend of grabens (e.g. Rønne Graben). The outline of this tectonostratigraphic unit can be also defined by differences in the Tectonostratigraphy to the surrounding areas. Even though the structure have been described (e. g. Seidel, 2019, Mazur et al., 2017, Mazur et al., 2015), no standardised definition of the outline of this tectonostratigraphic unit has been made to date. The extent of this tectonic unit was newly created/generalised with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Teisseyre-Tornquist Zone (TTZ)
The Teisseyre-Tornquist Zone (TTZ) is generally regarded as a fossil plate boundary in Europe that extends 2000km from the Baltic Sea to the Black Sea (Mazur et al., 2015). The suture is presumed to separate the East European Craton (EEC) from the Paleozoic terranes of Western Europe. In the Paleozoic to Mesozoic cover of this presumed suture zone a complex fault-system developed during the Mesozoic. This major fault system shows different characteristics at different times and shows both extensional structures (Most of Triassic until Jurassic), strike-slip elements (Permian, partly within the Mesozoic?) and contractional to transpressive structures (Upper Cretaceous).
Rønne Graben
Rønne-Graben
We describe the "Rønne Graben" as a tectonic unit, whose boundaries are mainly defined by faults and the extend of graben. The outline of this tectonostratigraphic unit can be also defined by differences in the tectonostratigraphy to the surrounding areas. Even though the structure have been described (e. g. Seidel, 2019), no standardised definition of the outline of this tectonostratigraphic unit has been made to date. This tectonic unit is listed here only for completeness and is not part of German territory. The extent of this tectonic unit was newly created/generalised with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also „Tectonic boundaries in Germany”.
NNE-SSW stiking transfer element between the Sorgenfrei-Tornquist Zone and the Teisseyre-Tornquist Zone (e.g. Liboriussen et al., 1987)
We describe the Kolobrzeg Block as a tectonic unit, whose boundaries are mainly defined by faults. The outline of this tectonostratigraphic unit can be also defined by differences in the tectonostratigraphy to the surrounding areas. Even though the structure have been described (e. g. Seidel, 2019; Kosakowski et al., 2010), no standardised definition of the outline of this tectonostratigraphic unit has been made to date. This tectonic unit is only listed here for the sake of completeness and only a small part of it lies on German territory. The extent of this tectonic unit was newly created/generalised with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Kolobrzeg Block
The Kolobrzeg block is a tectonic block of the northwestern Teisseyre-Tornquist zone.
We describe the Gryfice Block as a tectonic unit, whose boundaries are mainly defined by faults. The outline of this tectonostratigraphic unit can be also defined by differences in the tectonostratigraphy to the surrounding areas. Even though the structure have been described (e. g. Seidel, 2019; Kosakowski et al., 2010), no standardised definition of the outline of this tectonostratigraphic unit has been made to date. The extent of this tectonic unit was newly created/generalised with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Gryfice Block
The Gryfice Block is one major block, that belongs to the TTZ. It is bordered by the Adler Kamien fault zone to the southwest and in the north by the Rønne Graben (GRAVERSEN 2004). According to DADLEZ (2003) and KIERSNOWSKIE & BUNIAK (2006), the block continues in southeast direction as part of the onshore Mid Polish Trough or Pomeranian Segment.
Pernille fault
Gryfice fault zone
The Gryfice fault zone is located above a Palaeozoic high (Seidel 2019). This high is probably formed by Rotliegend volcanics or an unidentified tilted horst block. The fault zone strikes NW towards the Skurup Fault. It is formed by five major subparallel fault planes. One is located within the Palaeozoic strata and connected to the Palaeozoic high. The assumed rotated block might be bordered to the east by the northeastward dipping GRY_deep fault plane.
Swabian - Franconian - South Thuringian Block
We describe the Swabian - Franconian - South Thuringian Block as the sum of neighbouring tectonostratigraphic structural units, whose boundaries are defined by faults and/or on the base of partly fuzzy trends of the lithofacies and paleofacies. The extent of this tectonostratigraphic units was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: Röllig et al. (1990), GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1536). For References see also Tectonic boundaries in Germany.
Southern Franconian - Swabian Escarpments
We describe the Southern Franconian - Swabian Escarpments as a tectonostratigraphic unit, whose boundaries are defined by faults and/or on the base of partly fuzzy trends of the lithofacies and paleofacies as well as geomorphological aspects. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
The Southern Franconian-Swabian Escarment subdomain is characterized by long-distance impact of the Alpine orogeny and by the long living, ENE striking lineaments such as the Schwarzwald-Bayerwald line. [Domain type: Deformed sedimentary overburden, Basement: Moldanubian.]
Freudenstadt-Hohenzollern-Filder-Bodensee Graben system
We describe the Freudenstadt-Hohenzollern-Filder-Bodensee Graben system as a cluster with intersecting Cenozoic-Quaternary faults. The outline frames the occurence of the fault of the graben system. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:1000000. For References see also Tectonic boundaries in Germany.
Southern Kraichgau Depression & Franconian Platform subdomain
We describe the Southern Kraichgau Depression & Franconian Platform subdomain as a tectonostratigraphic unit, whose boundaries are only in sections defined by faults but also are defined on the base of partly fuzzy trends of the lithofacies and paleofacies. The extent of this unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1356). Map Reference: GK 1:1000000, GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1356). For References see also Tectonic boundaries in Germany.
Domain type: sedimentary overburden, Basement: Mainly Saxothuringian.
German Alps
We describe the German Alps as a superordinate tectonostratigraphic basement, unit, whose boundaries are defined by faults (thrusts) and lithological changes. It's a combination of tectonostratigraphic units, which show predominantly Alpidic deformation structures. The subdivision of this domain is based on the Austrian subdivision for the HIKE project. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), GK 1:1000000. For References see also Tectonic boundaries in Germany.
The structural units of the European Alps consist of the Helvetic, the Penninic, the Ostalpin and the Südalpin. The Bavarian Alps consist of the superordinate units of Folded Molasse (Faltenmolasse) with upright Molasse, the Helvetic, the Ultra-Helvetic, the Feuerstätter Flysch, the Rhenodanubikum, the Arosa zone and the Northern Calcareous Alps (Nördliche Kalkalpen) (Fig. 18). Due to Upper Cretaceous´ nappe and flake tectonics, reverse-and thrust faults, strike slip but also normal faults were formed, which separate at the same time the nappes and flakes. The W-E to WSE-ENE running fault zones separate the individual nappes, and often are transferred by NW-SE and NE-SW running strike slip fault. Prominent examples At diagonal and transverse fault systems (lateral ramps, strike-slip faults) the geometry of folds and thusts often changes abruptly in the strike, whereby the amount of the total shortening between individually often differently deformed segments within an thrust belt (transfer faults) remain preserved and fault offset amounts of up to several kilometers can add up. Further characteristics for the structural style are strike-slip fault systems and associated compressional- and extensional structures. These were formed during Oligocene-Miocene N-S compression caused by eastward directed shift of the central East-Alp block. Examples for these fault systems are Innsbruck-Salzburg-Amstetten fault Salzach–Ennstal fault, Königsee–Traunsee fault.[Domain type: Cenozoic basement block, Basement: Moldanubian /Alpine orogeny.]
Rhenodanubian Flysch
Rheno Danube Flysch
The Rhenodanube-Flysch subdomain belongs to the Helveticum-Arosa zone of the Alps. Domain: Cenozoic basement block, Basement: Moldanubian/Alpine orogeny.
The here used extent of this structural unit is based on Freudenberger & Schwerd (1996). The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Folded Molasse Basin
Königsee-Traunsee fault system
The Königsee-Traunstein fault system is located within the Staufen-Höllengebirge Nappe and borders to the Hallstätter Nappe in the north. The fault system extends over c. 20 km and runs WSE-ENE.
The here used extent of this structural unit is based on Freudenberger & Schwerd (1996). The exact definition of the fault domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Northern Calcerous Alps (Bavarian Nappe System)
The extent of this structural unit is based on Freudenberger & Schwerd (1996). The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Helveticum
We describe the Rynkøbing-Fyn-Møn-Arkona highs as a WNW-ESE striking chain of highs in the north of the Southern Permian Basin. Here we define this chain of structural highs as a tectonostratigraphic domain whose boundaries are not clearly defined by faults and fault systems. The outline of the domain can only be roughly defined based on lithostratigraphic trends and on the base of differences in the deformation pattern and differences of the erosional level to surrounding areas. Even though the structure have been described (e. g. Doornenbal & Stevenson, 2010), no clear definition of the outline of this tectonostratigraphic unit has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Rynkøbing-Fyn-Møn-Arkona highs
The Ringkøbing-Fyn High separates the Danish subsurface into the Norwegian-Danish Basin to the north and the North German Basin to the south. The Ringkøbing-Fyn High consists of relatively shallow basement rocks as compared to the Norwegian-Danish Basin which is cut by the approximately north-south trending Horn Graben. The western fraction of the high is bounded by the Central Graben in the West and the Horn Graben in the East which is characterized by ESE-WNW to E-W to ENE-WSW to NE-SE trending extensional faults, displaying half-graben structural settings (Javed, 2012).
We describe the Møn-Arkona High as part of a WNW-ESE striking chain of highs in the north of the Southern Permian Basin. Here we define Møn-Arkona High as a tectonostratigraphic unit, whose boundaries are not clearly defined by faults. The outline of this tectonostratigraphic unit can be also defined based on lithostratigraphic trends and on the base of differences in the deformation pattern and differences of the erosional level to surrounding areas. Even though the structure have been described (e. g. Seidel, 2019), no clear definition of the outline of this tectonostratigraphic unit has been made to date. The extent of this tectonic unit was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
Møn-Arkona High
The Møn-Arkona high domain represents a summary of the Møn High and Arkona High, both located in the Baltic Sea and is associated to the Ringkøbing-Fyn High. Domain type: Paleozoic basement high below relatively thin Cenozoic/Cretaceous to Mesozoic (?) sedimentary coverage, Basement Domain: Baltica.
Juetland-Moen fault zone
The Jütland‐Møn fault zone forms WNW striking steps of the southwestward dipping crust of Baltica (EEC) and its Late Proterozoic to Early‐Palaeozoic cover, below the thick (500‐2500 ms) thrust and folded Ordovician. According to Seidel (2019) the fault zone belongs to basement faults, which are responsible for the stepwiese southwestward dipping of Baltica. The fault zone can be traced over 70 km from the Adler‐Kamień Fault Zone (DE-9017) in a WNW direction, dipping towards SSW. Seven separate single normal fault planes can be traced: Jütland‐Møn 1‐4, Basement_step 1, 4 & 5 . The vertical displacement reaches up to 600 ms, but decreases towards the WNW to an offset of about 100 ms.
Binz Hamrane fault
The NNE-SSW-running Binz-Hamrane fault probably has a strike slip character (Seidel 2019) and is located NE of Rügen.
Basement step I
Basement step II
Basement step III
Basement step IV
Hiddensee fault
NNE-SSW running normal fault in northern extension of isle of Rügen that belongs to basement faults, which are responsible for the stepwise southwestward dipping of Baltica (Seidel 2019).
Basement step V
Arkona fault
The WNW-ESE striking Arkona fault is a normal fault, characterized by no massive offsets and partially formed as a flexure. This fault belongs to Paleozoic-Mesozoic faults whtin the accretionaly wedge and younger overlying successions (Seidel 2019).
Agricola Svedala fault II
Bohemian Massif & East German Variscan to Pre-Variscan basement highs
We describe the Bohemian Massif & East German Variscan to Pre-Variscan basement Highs as tectonostratigraphic basement units, whose boundaries are defined by faults and/or lithological changes. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: Röllig et al. (1990), GK 1:1000000. For References see also Tectonic boundaries in Germany.
[Domain type: Variscan basement block, Basement: Saxothuringian.]
Bavarian - Bohemian Teplá-Barrandian
We describe the Bohemian (Teplá-Barrandium) block as a tectonostratigraphic basement unit, whose boundaries are defined by faults and lithological changes. It's a combination of the Tepla-Barrandium basement rock outcrops of the Bavarian Forest and the Bohemian Massif. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Besides the presented generalized overview fault-data (Schulz et al., 2013), the geological state authority of Bavaria (LFU) provides and describes a more detailed and partly updated fault data set of Bavaria within the framework of the HIKE project (DE-BY_1531). Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), HIKE (DE-BY 1531). For References see also Tectonic boundaries in Germany.
SE Central Netherlands Basin domain
The extent of the Cenozoic tectonostratigraphic domain was newly created with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. For References see also Tectonic boundaries in Germany.
The SE Central Netherlands basin domain is a Mesozoic basin west of the Münsterland Cretaceous basin and is characterized by WNW-ESE striking faults. During the Paleocene Laramide inversion, the West and Central Netherlands basins were both further uplifted and deeply eroded, locally down to the Triassic (Wong et al., 2007). The Subhercynian inversion in the Central Netherlands Basin is less well documented, as due to deep erosion during later phases no Upper Cretaceous deposits are preserved, but also there in several wells Danian chalk overlies pre-Cretaceous successions (Wong et al., 2007). [Domain type: Sedimentary overburden, Basement: Avalonia.]
The European Molasse Basin is a Tertiary foreland basin at the northern front the Alps and extends over parts of France, Switzerland, Germany and Austria and was build some 35 Million years ago. This large asymmetrical syncline is filled with mostly clastic sediments originating from erosional processes of Alps, and is underlain by Mesozoic sedimentary successions. The typically wedge shape of the basin evolved in consequence of the Euro-Adriatic continental collision and the rise of the Alps since the Cretaceous (Berge and Veal 2005). Those sediments are partly overrun and folded due to the ongoing plate movement of the Euro-Adriatic continental collision (Schmid et al. 2008). In general, foreland basins are known to contain complex fault pattern due to the tectonic development (Beaumont 1981, Decelles & Giles 1996) and are characterized by thrusts close to the deformation front due to plate convergence and normal faults at the foreland, due to extensional stresses, which lead to basin subsidence foreland bulge development (Bergerat 1987, Bradley & Kidd 1991). Example for this complexity of fault pattern also within the South German Molasse basin are recent studies on a 3D seismic cube around Munich (von Hartmann et al. 2016). Here, large normal faults show lateral alternating dips that displace the Molasse sediments. Although they are disconnected, they strike parallel to fault lineaments of the underlying carbonate platform. Von Hartmann et al. (2016) suggest that these faults grew both upward and downward from the middle of the Molasse package, are newly initiated within the Molasse sediments and not caused by reactivation of the faults in the carbonate platform and/or crystalline basement. Aside from these locally observed characteristics, main structural elements in the South German Molasse (Fig. 17 a, country sheet) are found in the North the “Folded Molasse (directly in front of the Alps and therefore involved within the nappes), which is bordered by the Alpen Randstörung. North of this fault the so called “Foreland Molasse is located, which only is characterized by nearby horizontal bedding, flexures and joints. Prominent fault elements are the Landshut-Neuöttinger fault, Donaurandabbruch and the Keilberg fault (Fig. 17 b, country sheet). Domain type: Cenozoic foreland basin, Basement: Moldanubian.
South German Molasse Basin
We describe the South German Molasse Basin as a tectonostratigraphic unit in the northern foreland of the Alps. To the south this tectonostratigraphic domain is borderd by thrusts of the Folded Molasse. However, the actual structure is a result of erosion and especially to the north a discrete outline cannot be clearly defined. The extent of this unit was edited with a view to a structured assignment of fault data for the HIKE project and is based on a large number of partly contradictory map series and citations that were generalized for this purpose. The exact definition of the domain borders and the remaining uncertainties therein in some areas is still to be described/discussed in detail in the future. Due to increased exploration within this region for hydrocarbons, and in recent years also for geothermal energy, a large amount of seismic data (also 3D) has been collected. In recent years, new interpretations have been carried out based on this data and new fault maps have been developed. Since the generalized fault dataset (Schulz et al., 2013) presented here contains datasets older than the 1990's, some lineaments contradict the latest findings. The most up-to-date data for this region, with a higher level of detail, is provided by the LFU for Bavaria in the Hike project. Map Reference: Map Reference: GK 1:500000 of Bavaria (Freudenberger & Schwerd, 1996), tectonic map of Bavaria 1:1000000 (Freudenberger & Schwerd, 1996), GK1000, HIKE (HotLime_Case_Study_1). For References see also Tectonic boundaries in Germany.
Landshut-Neuöttinger Escarpment
The Landshut-Neuötting fault zone, located in front of the Donau-Randabbruch fault zone, borders the crystalline of the Landshut-Neuötting high towards SW. The fault zone has a length of c. 50 km and runs WNW-ESE.
Pfullendorf fault system
WSW-ENE-running fault of a length of < 40 km located in the western area of the South German Molasse Basin.
Keilberg fault
The c. 40 km long, NNW-SSE-running Keilberg fault displaces the Bohemian Massif up to 1200 m against the South German Großscholle.
Lauchert graben fault system
The c. 13 km long, N-S-running Lauchert graben fault system is located at the NW-margin of the South German Molasse basin and close to the Hohenzollern graben fault system.
Donau Escarpment
Northeastern boundary of the Southern Molasse Basin and simultaneous southwestern boundary to the Bavarian Forest, running WNW-ESE with a length c. 130 km. At this fault zone, the basement of the Bavarian Forest has been uplifted by more than 1300 m (Rohrmüller et al. 1996) compared to its foreland and locally a fault zone width of 5 km has been documented (Führer & Soffel 1975). The fault was initiated during the Variscan orogeny about 330 million years ago. During Alpidic orogeny, the fault was reactivated, especially from the Cretaceous until the Tertiary. The Danube rim fault has a jump
Schwarzwald-Bayerwald fault zone
The Schwarzwald-Bayerwald fault zone represents the western extension of the Donau Escarpment and is located at the N-margin of the South German Molasse Basin. The W-E-running fault zone often shows minor fault throws of 10-30 m, very locally up to 70 m (Walter 1995) and extends over a lenght of < 20 km.
Tectonic Boundary in Ukraine
Тектонична границя в Україні
All named tectonic boundary objects that are located (at least partly) in Ukraine, are identified by an ID with the prefix „UA“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Ukraine displayed in the HIKE European fault database, taken from the tectonic map of Ukraine 1:1.000.000
Fault systems of the Ukrainian shield
Система розломів Українського щита
Fault systems of the Ukrainian shelf are limited by the Prychernomorska Lowland to the south, The river Prypyat and its tributaries to the north, Prydniprovska Lowland to the east and the Volynska and Podilska Uplands to the west
Системи розломів українського шельфу обмежені Причерноморською низовиною на південь, річкою Прип'ять та її притоками на півночі, Придніпровською низовиною на сході та Волинською та Подільською височинами на заході
Тетерівський
The fault zone is traced from Hrytsiv town in the southwest to the river Pripyat in the northeast (on the border with Belarus) and passes into the territory of this country.
Зона розлому стежиться від м. Грицев на південному заході до річки Прип´ять на північному сході ( на кордоні з Білоруссю) і переходить на територію цієї країни
Teterivsky Fault (418)
Chernobylskyi Fault
Чорнобильський
From Bila Krynytsia village in the south-west it is traced in the north-eastern direction to Chornobyl city
Від селища Біла Криниця на південному заході трасується в північно-східному напрямку до м. Чорнобиль
Loevsky Fault
Лоєвський
Nemyrivsky Fault
Traces from the Dniester River near Mohyliv-Podilskyi town in the southwest to the Yadlovo-Traktemirovska fault zone in the north-eastern direction to Berezan town
Трасується від р. Дністер поблизу м. Могилів-Подільський на південному заході до Ядлово-Трактеміровської зони розломів в північно східному напрямку на м. Березань
Бузький
It is traced from Bershad town on the south-east to the intersection with the Nemyrivskyn fault near Nemyriv town on the north-west.
Стежиться від м. Бершадь на ПдСх до перетину з Немирівським розломом біля м. Немирів на ПнЗх
Khmilnyкsky Fault
Хмільникський
Buzky Fault (255)
Zvizdal-Zalіsky Fault
Звіздаль-Заліський
Observed from Ilyintsi village in the south to the Andrushivky fault in the north near Andrushivka village
Спостерігається від с. Ільїнці на півдні до Андрушівського розлому на півночі поблизу селища Андрушівка
Odesko-Talnivsky deep fault zone
без назви
Chip-type faults to the Odesko-Talnivsky deep fault zone near Haivoron town
Розломи сколового типу до Одесько-Тальнівської зони глибинного розлому поблизу м. Гайворон
Letychivsky Fault
Летичівський
Followed from Shpykov village in the southeast to the river Sluch near Starokostiantyniv town in the northwest
Стежиться від с. Шпиков на південному сході до річки Случь поблизу м. Старокостянтинів на північному заході
Bershadsky Fault
Бершадський
It can be traced from Bershad in the southwest to the Nemyrivsky fault near Shpykov village in the northwest
Простежується від м Бершадь на південному заході до Немирівського розлому поблизу селища Шпиков на північному заході
Брусилівський
It is traced from Skvira town in the south to Kornin village in the north
Стежиться від м. Сквіри на півдні до селища Корнін на півночі
Brusylivsky Fault (247, 248)
Tsentralny Fault
Центральний
It is traced in the submeridional direction in the form of fragments from the village of Kornin in the south and is cut by the Teterivsky fault in the north near the country's border.
Стежиться в субмеридіональному напрямку у вигляді фрагментів від селища Корнін на півдні і зрізається Тетерівським розломом на півночі біля кордону країни
Boguslavsky Fault
Богуславський
Brusylivsky Fault (243)
Sushchansko-Perzhansko-Surozkyi Fault
Сущано-Пержансько-Сурозький
Kry Faultvorizhsko-Kremenchutsky Fault
Криворізько-Кременчуцький
Within the USh is traced from Snihurivka village in the south to the border of DDZ in the northeast (Nov.Galeshchyna village) and further to the northeast in the EEP foundation
В межах УЩ трасується від с. Снігурівка на півдні до границі ДДЗ на північному сході (с. Нов.Галещина) і далі на північний схід у фундаменті СЄП
Zakhidnoinguletsky Fault
Західноінгулецький
In the south near the settlement of Bila Krynytsia it is limited by the Kryvorizhsko-Kremenchugsky deep fault, in the north near Hradynsk village it is blocked by DDZ deposits.
На півдні в районі селища Біла Криниця обмежений Криворізько-Кременчуцьким глибинним розломом, на півночі поблизу селища Градинськ перекривається відкладами ДДЗ
Ky Faultrovogradsky Fault
Кіровоградський
t is observed in the form of a tectonic zone from Bashtanka town in the south, through Kropyvnytskyi (Kirovohrad) city and further in the area of ​​ Zolotonosha town in the north.
Спостерігається у вигляді тектонічної зони від м. Баштанка на півдні, через м. Кропивницький (Кіровоград) і далі в районі міста Золотоноша на півночі стежиться у фундаменті ДДЗ
Kirovogradsky Fault
It is observed in the form of a tectonic zone from Bashtanka town in the south, through Kropyvnytskyi (Kirovohrad) city and further in the area of Zolotonosha town in the north.
Pervomaisky Fault (422)
Первомайський
Traces from Mykolayiv in the southeast to Pervomaisk in the northwest
Трасується від м Миколаїв на південному сході до м. Первомайськ на північному заході
Talnivsky Faulti
Тальнівський
It is traced from the Sinitsa River (east of Gaivoron town to Talne village on the Girsky Tikich River
Стежиться від р. Синиця (на схід від м. Гайворон до селища Тальне на р. Гірський Тікич
It is traced from Bershad town on the south-east to the intersection with the Nemyrivsky fault near Nemyriv town on the north-west.
Khmіlnyksky Fault
Buzky Fault (420)
Сарненсько-Варварівський
Sarnensko-Varvarivsky Fault (413)
Andrushivsky Fault
Андрушівський
It is traced in the sublatitudinal direction from Hrytsev village in the west to the Boguslav submeridional fault near Kornin town in the east
Стежиться в субширотному напрямку від селища Грицев на заході до Богуславського субмеридіонального розлому біля містечка Корнін на сході
Sarnensko-Varvarivsky Fault (410)
Suschano-Perzhansky Fault
Сущано-Пержанський
North-eastern continuation of the Kremenetsky fault within the USh from the river Sluch (Sosnove village) to the border of Ukraine and further to the territory of Belarus
Північно-східне продовження Кременецького розлому в межах УЩ від річки Случь (с. Соснове) до кордону України і далі на територію Білорусі
Mushketivsky Fault
Мушкетівський
Konksky Fault (353, 354, 355)
Конкський
The system of sublatitudinal faults is limited by the Kryvorizhsko-Kremenchugky fault in the west and at the latitude of Kamyanka-Dniprovska is limited by the Malokaterynivka fault.
Система субширотних роломів обмежується Криворізько-Кременчуцьким розломом на заході і на широті м. Кам’янка-Дніпровська обмежується Малокатеринівським розломом
Khortytsky Fault (344)
Хортицький
Traced from the shore of the ​​Azov Sea near Berdyansk in the north-western direction to Malokaterynivka village
Трасується від берега Азовського моря неподалік м. Бердянськ в північно-західному напрямку до селища Малокатеринівка
Azovo-Pavlogradsky Fault
Азово-Павлоградский
Within the USh it is observed from Milky estuary on the coast of the Azov Sea in the south to Pavlograd city in the north
В межах УЩ спостерігається від Молочного лиману на березі Азовського моря на півдні до м. Павлоград на півночі
Dzerzhinsky Fault
Дзержинський
Traces from the Derezuvatsky fault in the southeast (Solone village ) to Verkhnodniprovsk town in the northwest
Трасується від Дерезуватського розлому на південному сході (с.Солоне) до містечка Верхньодніпровськ на північному заході
Kommissarivsky Fault
Комісарівський
It can be traced from Zhovti Vody town on the south-west in the direction of Verkhnodniprovsk city
Простежується від м. Жовті Води на ПдЗх в напрямку м. Верхньодніпровськ на ПнСх
Verkhivtsevsky Fault
Верхівцевський
Faults of the South Donbass block tectonic zone
Розломи Південнодонбаської брилової тектонічної зони
Fault-type faults are common in the southern part of Donbass from Kurakhove town in the west to Amvrosiyivka in the east
Розломи скидового типу поширені в південній частині Донбасу від м. Курахове на заході до м. Амвросіївка на сході
Оріхово-Павлоградський
Within the USh it is traced from Melitopol city in the south-west in the direction of Orikhiv and further with a change in the direction of north-west to Pavlograd with continuation in the foundation of DDZ
В межах УЩ трасується від міста Мелітополь на південному заході в напрямку м. Оріхів і далі зі зміною напрямку па ПнЗх до м. Павлоград з продовженням у фундаменті ДДЗ
Orikhovo-Pavlogradsky Fault (459)
It is bounded by the Teteriv fault in the south near the town of Polonne and runs north, northeast to the village. Gorodnitsa
Обмежений Тетерівським розломом на півдні в районі містечка Полонне і трасується північ, північний схід до с. Городниця
Konksky Fault (319)
Brusylivskyi Fault (456)
It is traced in the submeridional direction in the form of fragments from Kornin village in the south and is cut by the Teterivsky fault in the north near the country's border.It is bounded by the Teterivsky fault in the south near Polonne town and runs north, northeast to Gorodnitsa village
Дерезуватський
Within the USh is traced from Kalinovske village in the south-west in the direction of Nikopol, Ordzhonikidze and is limited by the system of faults of the Orikhovo-Pavlograd fault in the northeast (east of Novomoskovsk)
В межах УЩ трасується від с. Калинівське на південному заході в напрямку на м. Нікополь, Орджонікідзе і обмежується системою розломів Оріхово-Павлоградського розлому на північному сході (на схід від м.Новомосковськ)
Derezuvatsky Fault (312)
y Faultemilchy Faultnsky Fault
Ємильчинський
It is traced from the Teterivsky fault in the south-east (Bykivka village) to the Sushchano-Perzhansky fault in the north-east (near Olevsk).
Стежиться від Тетерівського розлому на південному сході (с. Биківка) до Сущано-Пержанського розлому на північному сході (поблизу м. Олевськ)
Traced from the shore of the Azov Sea near Berdyansk in the north-western direction to Malokaterynivka village
Khortytsky Fault (311)
Pervomaisky Fault (449)
Derezuvatsky Fault (310)
Девладівський
It is bounded by the Kryvorizhsko-Kremenchugsky fault in the west (near Gleyuvatka village), in the east by the Orikhovo-Pavlogradsky fault (near Novomykolayivka village).
Обмежений Криворізько-Кременчуцьким розломом на заході (біля с. Глеюватка), на сході - Оріхово-Павлоградським розломом (біля с. Новомиколаївка)
Devladivsky Fault (306)
Orikhovo-Pavlogradsky Fault (304, 340)
Smelyansky Fault
Смелянский
Zakhidno-Inguletsky Fault
Західно-Інгулецький
Inguletsky Fault
Інгулецький
In the south it is limited by the Bokovyansky fault, in the north it can be traced outside the USh (with Globyne) in the DDZ foundation
На півдні обмежений Боковянським розломом, на півночі простежується і за межами УЩ (с Глобине) у фундаменті ДДЗ
Bokovy Faultansky Fault
Боковянський
Bounded in the southeast by the Kryvorizhsko-Kremenchugsky deep fault near Kryvyi Rih city, in the northwest it subsides near Rotmistrovka village.
Обмежений на південному сході Криворізько-Кременчуцьким глибинним розломом неподалік м. Кривий Ріг , на північному заході затухає поблизу селища Ротмістровка
Odeskyi Fault (474)
Одеський
Within the USC stretches from the village of Tsebrykovo in the south in a northerly direction to the town of Blagoveshchensk (Ulyanovka) Cherkasy region
В межах УЩ простягається від селища Цебриково на півдні в північному напрямку до містечка Благовіщенське (Ульянівка) Черкаської області
Odeskyi Fault (473)
Within the USh stretches from Tsebrykovo village in the south in a northerly direction to the town of Blagoveshchensk (Ulyanovka) town Cherkasy region
Teterivsky Fault (472)
Traced from Nemyriv town in the southeast through Khmilnyk town and is limited by the Volodymyr-Volynsky fault near the village of Hrytsev village in the northeast.
Трасується від м. Немирів на південному сході через м. Хмільник і обмежується Володимир-Волинським розломом поблизу селаща Грицев на північному сході.
Субоцько-Мошоринський
Traced in the sublatitudinal direction, bounded by the Zvenigorodsko-Annivsky fault in the west (at the latitude of Novoarkhangelsk), in the east – Kryvvorizhsko-Kremenchugsky
Трасується в субширотному напрямку, обмежений Звенігородсько-Аннівським розломом на заході (на широті м. Новоархангельск), на сході - Криворізько-Кременчуцьким
Derezuvatsky Fault (436, 437)
Within the USh is traced from Kalinovske village in the southwest in the direction of Nikopol, Ordzhonikidze and is limited by the system of the Orikhovo-Pavlogradsky fault in the northeast (east of Novomoskovsk town)
Zvenigorodsko-Annivsky Fault
Звенігородсько-Аннівський
Traces from Snihurivka vilage in the southeast to the Pervomaisky fault at the foot of the mountain Tikich
Трасується від селища Снігурівка на південному сході до Первомайського розлому біля гирла р. Гірський Тікич
Orikhovo-Pavlogradsky Fault (435)
Tsentralno-Buzky Fault
Центрально-Бузький
Bounded by the Pervomaisk fault near the city of Pervomaisk in the southeast and Talnivsky in the northwest
Обмежений Первомайським розломом поблизу м. Первомайськ на південному сході та Тальнівським на північному заході
Malokatery Faultnivsky Fault
Малокатеринівський
Within the limits of USh it is traced from N. Sirogoza village in the southwest to Devladovsky fault in the northeast near Novomykolayivka village
В межах УЩ стежиться від селища Н. Сірогози на південному заході до Девладовського розлому на північному сході в районі селища Новомиколаївка
Voznesensky Fault
Вознесенський
Observed from Voznesensk on the south-west to Pidhorodnia on the north-west, where it is cut by the Pervomaisky fault
Спостерігається від м. Вознесенськ на ПдСх до м. Підгородня на ПнЗх, де зрізається Первомайським розломом
Derezuvatsky Fault (433)
Pervomaisky Fault (266, 280)
Pervomaisky Transfer Fault
Без назви
Local transverse faults to the Pervomaisky fault in the section from Nova Odesa on the south-east to Voznesensk on the north-west
Локальні поперечні розломи до Первомайського розлому на ділянці від м. Нова Одеса на ПдСх до м. Вознесенськ на ПнЗх
Vradievsky Fault
Врадієвський
Within the limits of the USh it is traced from the sources of the Berezan river in the south-east in the direction of Vradiyivka town in the north-west.
В межах УЩ стежиться від витоків р. Березань на південному сході в напрямку м. Врадієвка на північному заході
Gvozdavsky Fault
Гвоздавський
It is traced from Berezivka town on the south-west Lyubashivka town on the north-west, where it is cut by the Odesky fault
Стежиться від м. Березівка на ПдСх до м. Любашівка на ПнЗх, де зрізається Одеським розломом
Dashevsky Fault
Дашевський
It is bounded on the southeast by the Talnivsky deep fault, and on the northwest by the Nemyrivsky fault near Illintsi village.
Обмежений на південному сході Тальнівським глибинним розломом , на північному заході - Немирівським розломом в районі селища Іллінці
Pervomaisko-Traktemyrivsky Fault
Traces in the northern direction from Pervomaisk in the south to Novoarkhangelsk and further to Talne village in the north
Трасується в північному напрямку від м. Первомайськ на півдні до м. Новоархангельск і далі до селища Тальне на півночі
Yadlovo-Traktemirovsky Fault (265)
Ядлово-Трактемирівський
Ядлово-Трактеміровський
The fragment of the fault is traced from Gogolivna village in the south to the border of the country in the north-eastern direction to Pripyat town
Фрагмент розлому трасується від селища Гоголівна півдні до кордону країни в північно-східному напрямку на м.Прип´ять
Yadlovo-Traktemirovsky Fault (448)
It is traced in the submeridional direction in the form of fragments from Kornin village in the south and is cut by the Teteriv fault in the north near the country's border.
Brusylivsky Fault (447)
Devladivskyi Fault (445)
South Donbass block tectonic zone
Південнодонбаська брилова тектонічна зона
Fault-type faults are common in the southern part of Donbass from Kurakhove in the west to Amvrosiyivka in the east
Korsatsky Fault
Корсацький
Within the USh it is observed from Primorsk city in the south and is limited by the Azovo-Pavlogradsky fault in the northwest
В межах УЩ спостерігається від м. Приморськ на півдні і обмежений Азово-Павлоградським розломом на північному заході
The Carpathian fault systems
Система розломів Карпат
Fault systems of the Carpathian are limited by the river Dniester and its tributaries to the east and river Tisa and its tributaries to the west and by the Carpathian mountains to the north and to the south
Системи розломів Карпат обмежені річкою Дністер та її притоками на сході та рікою Тисою та її притоками на заході та Карпатами на півночі та на півдні
Krakovetsky Fault
Краковецький
Parashky Fault
Парашки
Stebnytsky Fault
Cтебницький
Gorodetsky Fault
Городецький
Skolivsky Fault
Сколівський
Slavsky Fault
Славський
Orivsky Fault
Орівський
Kalusky Fault
Калушський
Beregovy Fault
Береговий
Бердо-Нароль
Berdo-Narol Fault (381)
Bory Faultslavo-Pokutsky Fault
Бориславо-Покутский
Zakarpatsky Fault
Закарпацький
Rozhansky Fault
Рожанський
Peredkarpatsky Fault
Передкарпацький
Zeleno-Kamy Faultansky Fault
Зелено-Камянский
Chernivetsky Fault
Чернівецький
Stryisky Fault
Стрийський
Shepitsky Fault
Шепітський
Radekhivsko-Rogatynsky Fault
Радехівсько-Рогатинський
Oashsky Fault
Оашський
Rava-Rusky Fault
Рава-Руський
Pry Faultpannonsky Fault
Припаннонський
Fault systems of the Dnieper-Donetsk Rift
Система розломів Дніпровсько-Донецької западини
Fault systems of the Dnieper-Donetsk rift are located on the Poltavska plain and Prydniprovska lowland and are limited by the Pryazovska upland to the south-east and the Donetskyi ridge from the east, some water reservoir to the west and the river Dnieper and its tributaries to the north
Системи розломів Дніпровсько-Донецького рифту розташовані на Полтавській рівнині та Придніпровській низовині та обмежені Прязовською височиною на південному сході та Донецьким хребтом зі сходу, деякими водосховищами на заході та річкою Дніпро та його притоками на півночі
Faults of the southern marginal zone
Розломи південної крайової зони
Traced from Slavutych in the northwest to Volnovakha in the southeast
Простежуються від м.Славутич на північному заході до м. Волноваха на південному сході
Lutuginskyi
Лутугінский
Krasnorichinsky (on the border with the Folded Donbass), then the faults of the Northern side zone
Краснорічинський (на межі із Складчастим Донбасом), далі розломи Північної бортової зони
The Seversky Donets River in the southeast and the Dnieper River in the northwest are limited within the borders of Ukraine.
Обмежуються в кордонах України р. Сіверський Донець на південному сході та р. Дніпро на північному заході
Dniprovsko-Prypyatskyi
Дніпровсько-Припятський
Donetsko-Kadiivskyi
Донецько-Кадіївський
Korulsko-Krasnopilskyi
Корульсько-Краснопільський
Tsentralnyi Fault
Poliskyi Fault
Поліський
Tsentralno-Donetskyi Fault
Центрально-Донецький
Fault system of the North-Ukrainian hand zone
Система розломів Північно-української горстової зони
Traced in fragments in the sublatitudinal direction south of Ratne town to Kamin-Kashirsky
Трасується фрагментарно в субширотному напрямку південніше м. Ратне до м. Камінь-Каширський
Pivdennoratnivsky Fault
Південноратнівський
Fault system of the crystalline Basement
Система розломів кристалічного фундамента СЄП в ДДЗ
Orikhovo-Pavlogradskyi
Traced from Pavlograd in the southeast to the border with Russia in the northwest, passes by Sumy
Простежений від м. Павлоград на південному сході до кордону з РФ на північному заході, проходить повз м. Суми
Kryvorizhsko-Kremenchutskyi
Traced from Globyne village in the south through the DDZ in the northern, northeastern direction to the border with Russia in the area of Middle Buddha
Простежується від селища Глобине на півдні через ДДЗ в північному, північно-східному напрямку до кордону з РФ в районі с. Середина Буда
Yadlovo-Traktemirovsky
Continuation in the northern direction of the USH fault from the southern side of the DDZ near Gogoliv village to the Desna River in the north
Продовження в північному напрямку розлому УЩ від південного борту ДДЗ в районі селища Гоголів до річки Десна на півночі
Pereyaslav-Khmelnytskyi-Prylukskyi
Переяслав-Хмельницький-Прилуцький (Кіровоградський)
Traced according to geophysical data from Zolotosha town in the south to the border with Russia near Semenivka town in the north
Трасується за геофізичними даними від м. Золотоша на півдні до кордону з Росією поблизу м . Семенівка на півночі
Glukhivsky
Глухівський
Traces from the river Snov in the west to the border with Russia in the east in the direction of Rylsk
Трасується від річки Снов на заході до кордону з Росією на сході в напрямку м. Рильск
Kharkivsky
Харківський
Bounded in the south by the Kuibyshevsky fault east of Pereshchepyne village, in the northeast it extends beyond Ukraine to the north of Kharkiv
Обмежений на півдні Куйбишівським розломом східніше селища Перещепине, на північному сході виходить за межі Украіни на північ від м. Харків
Fault systems of the South Ukrainian monoclinal
Система розломів Південно-Української монокліналі
Fault systems of South Ukrainian monoklinal are located on the Prychernomorska lowland and limited by the Black sea and Azov from the south, the river Dniester from the west, the Pryazovska upland from the east and the Prydniprovska and the Podilska uplands from the north
Системи розломів південноукраїнського монокліналу розташовані на Причерноморській низовині та обмежені Чорним морем та Азовом з півдня, річкою Дністер із заходу, Приазовською височиною зі сходу та Придніпровською та Подільською височинами з півночі
Mykhailivskyi Fault
Михайлівський
Golitsynskyi Fault
Голіцинський
Odeskyi Fault
Traced according to geophysical data from Tsebrikovo villagre on the NW in the south-eastern direction near Odessa on the shelf of Zakhidnochornomorska depression
Трасується за геофізичними даними від селища Цебриково на ПнЗх в південно-східному напрямку повз м. Одеса на шельф Західно-Чорноморської западини
Khersonskyi Fault
Херсонський
Krakovetskyi Fault
Sulynsko-Tarkhankutskyi Fault
Сулинсько-Тарханкутський
Fault systems of the Pre-Dobruja
Система розломів Преддобруджи
Fault systems of the Pre-Dobruja are located on the Prychernomorska lowland and limited by the Black sea from the east and some lakes from the south, the river Dniester from the north and row of rivers from the east
Системи розломів Переддобруджі розташовані на Причерноморській низовині та обмежені Чорним морем зі сходу та деякими озерами з півдня, річкою Дністер з півночі та низкою річок зі сходу
Bystriiskyi Fault
Бистрівський
Kagul-Izmailskyi Fault
Кагул-Ізмаїльський
Fault systems of the Folded Donbass
Система розломів Складчастого Донбасу
Fault systems of the Folded Donbass are located on the Donetskyi ridge and are limited by the river Siverskyi Donets to the north-east and the Pryazovska upland to the south-west and row of rivers to the west
Системи розломів Складчастого Донбасу розташовані на Донецькому хребті і обмежені річкою Сіверський Донець на північному сході та Приазовською височиною на південному заході та низкою річок на заході
Donetsko-Kadiivskyi Fault
Traced from the town of Volnovakha in the southwest to the border of Ukraine in the direction of the village of Milerovo, Russia
Простежується від м. Волноваха на південному заході до кордону України в напрямку селища Мілерово Росії
Rovenkivskyi Fault
Донецько-Кадієвський
Traced from Volnovakhatown in the southwest to the border of Ukraine in the direction of Milerovo village, Russia
Pivnichno-Donetskyi Fault
Pivnichno-Donetskyi
Fault systems of the Crimea
Система розломів Криму
Fault systems of the Crimea are limited by Zakhidnochornomorska depression in the Black sea from the south and Sorokina depression from the east, the peninsula Crimea from the north and the Vylkivskyi shaft to the west
Системи розломів Криму обмежені Західночорноморською западиною в Чорному морі з півдня та Сорокинською западиною зі сходу, півостровом Крим з півночі та Вильківським валом на заході
Pivdennoberezhnyi Fault
Південнобережний
Zakhidno-Krymskyi Fault
Західно-Кримський
Fault systems of the Volyn-Podolian structure
Система розломів Волино-Подільської структури
Fault systems of the Volyn-Podolian structure are limited by the river Dniester and its tributaries to the west and south, the Poliska Lowland to the north and the Kievske plateau to the west
Cистеми розломів Волино-Подільської структури обмежені річкою Дністер та її притоками на захід та південь, Поліською низовиною на півночі та Київським плато на заході
Monastyrsky Fault
Монастирський
Andrushchivsky Fault
Андрущивський
Rivnensky Fault
Рівненьський
Dniprovsko-Prypyatsky Fault
Великомосиївський
Berzh-Baluchynskyi Fault
Берз-Балучинський
Podilsky Fault
Подільський
Kremenetsko-Perzhansky Fault
Кременецько-Пержанський
Berdo-Narol Fault (395)
Tovtrovy Fault
Товтровий
Suschano-Perzhansko-Kremenetsky Fault
Сущано-Пержансько-Кременецький
Bounded by the Prydnistrovskyi fault in the northwest near the Pomoriany village, on the northeastern flank near Koretsе town turns into Sushchano-Perzhansky fault
Обмежений Придністровським розломом на північному заході в районі селища Поморяни, на північно-східному фланзі в районі м Корець переходить в Сущано-Пержанський розлом
Кременецький
Povchano-Ustetskyi Fault
Повчано-Устецький
Troyanivsko-Gutsulsky Fault
Троянівсько-Гуцульський
Terebovlyansky Fault
Теребовлянський
Teterivsky Fault
Berezhansky Fault
Бережанський
Lutsky Fault
Луцький
Tektonische Grenzflächen in Bayern
Konzepte der in der Europäischen Störungsdatenbank im Detailierungsgrad von größer 1:200.000 gespeicherten und abrufbaren tektonischen Grenzflächen Bayerns, Stand 12/2020. Berücksichtig sind bedeutende Störungen und Störungssysteme in den geologischen Großeinheiten und strukturellen Domänen Bayerns, mit Ausnahme der Alpen, wie in verschiedenen Maßstäben kartiert oder aus indirekten Hinweisen unter Verwendung geeigneter Methoden abgeleitet. Diese Bestandsaufnahme zielt weniger auf eine vollständige Zusammenstellung wesentlicher tektonischer Elemente ab, als vielmehr auf die Betonung des kontextuellen Zusammenhangs des Störungs-Netzwerks, um das regionale tektonische Regime als Ergebnis großräumiger Krustenbewegungen zu erläutern. Die Erfassung tektonischer Elemente in Bayern und deren kontextuelle Klassifikation dauert an. Diese Bestandsaufnahme ist daher Gegenstand künftiger Fortschreibung. Diese „DE-BY“ Konzepte beschreiben das Störungsnetzwerk Bayern in einem höheren Detailierungsgrad als das deutschlandweite „DE“ Schema
Tectonic Boundaries in Bavaria
Concepts of tectonic boundaries in Bavaria, corresponding to scales of 1:200,000 and smaller, as stored in and retrievable from the European Fault Data Base, state 12-2020. Considered are major faults and fault systems from all geological units / structural domains of Bavaria, except for the German Alps Domain, as mapped in various scales or inferred from indirect evidence using various methods deemed appropriate in the respective geological settings. Rather than giving a full inventory of principal tectonic features, this compilation aims at stressing the contextual relationship of the fault network in order to elucidate the regional tectonic regime as the result of large-scale crustal movements. In Bavaria, tectonic boundary objects detection and contextual classification is an ongoing process. Hence, this inventory is subject to future upgrading and change. These “DE-BY” concepts, describe the Bavarian fault network at a level of detail beyond the Germany-wide scheme prefixed DE.
GC3D limits
.. here should be a short, 3-line text - describing the relevant scheme and allow the user to get started with the topic via the listed top concepts ..
Schichtstufenland Domäne (N und NW Bayern)
The tectonic boundaries of the sedimentary cover of the South German block, the Bavarian Scarpland, in parts can be directly observed, otherwise are extrapolated from outcrop evidence or inferred from contour lines pattern. The tectonic boundary inventory of the Scarpland presently is under revision and contextual classification. Many faults and fault zones, thus, are represented and described generalized, resembling a 1:1 m scale. The faults of Bavaria's small share of the Upper Rhine Graben subbasin Hanau-Seligenstadt Basin in the very northwest are described corresponding to a 1:50,000 scale.
Die Störungen im sedimentären Deckgebirge der Süddeutschen Großscholle, dem Bayerischen Schichtstufenland, sind hauptsächlich an der Oberfläche und in Aufschlüssen zu kartieren oder können aus Streichlinien-Mustern abgeleitet werden. Das Störungsinventar des Schichtstufenlandes ist derzeit in Überprüfung und kontextueller Klassifizierung. Viele der Störungen und Störungszonen sind daher nur generalisiert beschrieben und einem Maßstab entsprechend 1:1 Mio. dargestellt. Die Störungen des geringen bayerischen Anteils am Randbecken des Oberrheingrabens, der Hanau-Seligenstädter Senke, sind einem Maßstab von ca. 1:50 000 entsprechend beschrieben.
Die tektonischen Bauelemente der Süddeutschen Großscholle sind teils weitgespannte Aufwölbungen und Einmuldungen, teils weit durchziehende Bruchzonen. Die Störungen im sedimentären Deckgebirge, dem Bayerischen Schichtstufenland, streichen hauptsächlich in flach-herzynischer (WNW-ESE) bzw. steil-herzynischer oder fränkischer (NW-SE) Richtung und zeigen Anzeichen mehrphasiger Dehnung und Kompression (Graben und Horst). Die Verformungsstrukturen beinhalten Faltungen, Abschiebungen, Aufschiebungen und Überschiebungen.
Die tektonischen Bauelemente der Süddeutschen Großscholle sind teils weitgespannte Aufwölbungen und Einmuldungen, teils weit durchziehende Bruchzonen. Die Störungen im sedimentären Deckgebirge, dem Bayerischen Schichtstufenland, streichen hauptsächlich in flach-herzynischer (WNW-ESE) bzw. steil-herzynischer oder fränkischer (NW-SE) Richtung und zeigen Anzeichen mehrphasiger Dehnung und Kompression (Graben und Horst), zuletzt durch Reaktivierung während der saxonischen Bruchschollentektonik (Oberkreide bis Neogen), als Fernwirkung der alpidischen Gebirgsbildung. Die Verformungsstrukturen beinhalten Faltungen, Abschiebungen, Aufschiebungen und selten Überschiebungen.
2: Bavarian Scarpland domain (N and NW Bavaria)
Hersbruck Fault
Hersbruck Störung
W-E streichende Abschiebung mit Einfallrichtung N
W-E trending normal fault with dip direction N
Herrnneuses Fault
Herrnneuses Störung
SW-NE streichende Abschiebung mit Einfallrichtung NW
SW-NE trending normal fault with dip direction NW
Hassberg Fault
Hassberg Störung
NW-SE streichende Abschiebung mit Einfallrichtung NE
NW-SE trending normal fault with dip direction NE
Harres Fault
Harres Störung
Harrbach Fault
Harrbach Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW
NW-SE trending normal fault with dip direction SW
Hainbach Fault
Hainbach Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW (revers invertiert)
NW-SE trending normal fault with dip direction SW (reversly inverted)
Haidenaab Fault
Haidenaab Störung
NW-SE streichende Aufschiebung mit Einfallrichtung NE
NW-SE trending reverse fault with dip direction NE
Hanau-Seligenstadt Basin eastern margin
Erlensee-Alzenau Fault
New concept as of 2021-03-15, after the HIKE editorial deadline – no corresponding fault geometries in the HIKE Fault Data Base.
Neues Konzept von 2021-03-15, nach HIKE Redaktionsschluss – entsprechende Störungs-Geometrien in der HIKE Störungsdatenbank fehlen.
NNW-SSE trending, steeply WSW dipping normal fault featuring a throw of up to more than 200 m; northeastern boundary of Wilmundsheim Graben, a branch of Hanau-Seligenstadt Basin.
Erlensee-Alzenau Störung
Wilmundsheim Graben eastern boundary
N-S- trending, steeply W dipping normal fault; lower step of Anterior Spessart western boundary [DE-BY_1557], eastern boundary of Wilmundsheim Graben, a branch of Hanau-Seligenstadt Basin.
Wilmundsheim Graben Ostrand
Karlstein-Langstadt Fault
Western boundary of Stockstadt-Gross-Umstadt Block, the northern extension of Odenwald. On Bavarian territory, SW-NE trending, steeply NW dipping normal fault with a throw up to more than 200 m, offset 2 km to SE in between Kahl-Stockstadt Fault [DE-BY_1561] and Stockstadt-Obernburg Graben Fault [DE-BY_1574]. Here it forms the southeastern boundary of Kleinwelzheim Horst towards the Stockstadt-Obernburg Graben.
Karlstein-Langstadt Störung
Kahl-Kleinostheim Fault
NNW-SSE striking, steeply ENE dipping normal fault featuring a throw of up to 200 m; northeastern boundary of Kleinwelzheim Horst towards Wilmundsheim Graben, a branch of Hanau-Seligenstadt Basin.
Kahl-Kleinostheim Störung
Revised concept as of 2021-03-15, after the HIKE editorial deadline. Corresponding fault geometries in the HIKE Fault Data Base not adjusted accordingly.
Überarbeitetes Konzept von 2021-03-15, nach HIKE Redaktionsschluss. Die entsprechenden Störungs-Geometrien in der HIKE Störungsdatenbank wurden nicht angepasst.
Spessart-Odenwald Borderfault System
Spessart-Odenwald Randstörungssystem
Geknickt, insgesamt N-S streichende Abschiebung mit Einfallsrichtung ± W und westlich (sub)parallele ± E fallende Abschiebungen, die zusammen den Stockstadt-Obernburg Graben und Klingenberg Graben bilden.
Kinked, overall N-S trending normal fault with dip direction ± W paralleling a set of ± E dipping normal faults in the west, forming Stockstadt-Obernburg and Klingenberg Grabens.
Stockstadt-Obernburg Graben Eastern Flank
NNW-SSE to NNE-SSW trending, steeply WSW to WNW dipping normal fault forming the western scarp of Spessart mountains and the eastern boundary of Stockstadt-Obernburg Graben with main movement phases during Oligocene and Pliocene.
Stockstadt-Obernburg Graben Ostflanke
Obernauer Randverwerfung
Klingenberg-Graben
Paar NW-SE streichender Abschiebungen mit Einfallsrichtung zum Grabeninneren.
Pair of NW-SE trending normal faults with a inward graben dip.
Stockstadt-Obernburg Graben Western Flank
NNW-SSE to NNE-SSW trending, steeply ENE to ESE dipping normal fault featuring a throw of up to 150 m; western boundary of Stockstadt-Obernburg Graben with main movement phases during Oligocene and Pliocene.
Stockstadt-Obernburg Graben Westflanke
Randverwerfung Obernburg-Großostheim
Stockstadt-Obernburg Graben Fault
NNW-SSE trending fault running within Stockstadt-Obernburg Graben.
Stockstadt-Obernburg Graben-Störung
Spessart Borderfault
Spessartrand Störung
Insgesamt N-S streichendes System W fallender Abschiebung, bildet im nördlichen Abschnitt die Ostgrenze der Hanau-Seligenstädter Senke.
Overall N-S trending system of normal faults with dip direction W, in the northern part eastern boundary of Hanau-Seligenstadt Basin.
Anterior Spessart western boundary
N-S trending, veering to NNW-SSE in the south, main step of the Spessart Borderfault towards the Hanau-Seligenstadt Basin; continuing as Stockstadt-Obernburg Graben Eastern Flank [DE-BY_1575] in the south.
Vorspessart Randstörung
Spessartrandverwerfung
Spessartrandbruch
Hahnenkamm Scarp
N-S trending eastern branch of the Anterior Spessart western boundary.
Hahnenkamm Westabbruch
Michelbach Thrust
SW-NE striking, approx. 60° SE dipping thrust fault running from Wasserlos to Freigericht in Hesse; in sections northwestern boundary of Anterior Spessart basement swell.
Michelbach Überschiebung
Weiden Basin western margin
Westrand des Weidener Beckens
Western boundary of Weiden Basin, in its north towards the adjoining, buried and desintegrated remnants of Naab Basin Rotliegend deposits. Consisting of segments of, from N to S, Weidenberg Fault [LfU-BY_959], Birk-Stegenthumbach Fault [LfU-BY_1042], Fenkensees-Brüderes Fault [LfU-BY_1049] and the Freihung Fault System [LfU-BY_1388], plus an link between the faults, assumed due to the lack of borehole or seismic evidence.
Fenkensses-Brüderes Fault
Fenkensses-Brüderes Störung
N-S streichende Abschiebung mit Einfallrichtung E
N-S trending normal fault with dip direction E
Birk-Stegenthumbach Fault
Birk-Stegenthumbach Störung
Stegenthumbacher Störung
NNW-SSE streichende Abschiebung mit Einfallrichtung WSW (später aufschiebend invertiert)
NNW-SSE trending normal fault with dip direction WSW (later reversly inverted)
Freihung Fault System
Freihunger Störungssystem
Freihunger Störungszone
Von Kirchenthumbach bis zur Luhe Line [DE-BY_1387] bei Ehenfeld ziehende, NW-SE verlaufende, steil nach NE einfallendes Aufschiebungs-System mit einer (kumulativen) Sprunghöhe von bis zu mehr als 1,2 km. Mehrfach von Querstörungen versetzt und streckenweise als einzelne Groß-Aufschiebung ausgebildet. Im südlichen Abschnitt SW-Grenze der Weidener Bucht mit Rotliegend Ablagerungen.
Running from Kirchenthumbach to Luhe Line [DE-BY_1387] near Ehenfeld, NW-SE trending, steeply NE dipping system of reverse faults with a cumulative throw up to more than 1.2 km, in parts merging into one single reverse fault and offset by lateral faults. In its southern part, southwestern boundary of Weidener Bucht (Weiden embayment) of exposed/subcropping Rotliegend deposits.
Tanzfleck Fault
Tanzfleck Störung
Gewellt NW-SE verlaufende ca. 75° nach NE einfallende listrische Aufschiebung mit einen Vertikalversatz von etwa 400 m. Die Tanzfleck Störung zeigt eine ausgeprägte Abwärtsschleppung der Schichten der Liegendscholle, was eine zeitweise abschiebende Invertierung andeutet.
Undulate NW-SE trending approx. 75° NE dipping listric reverse fault with a throw of about 400 m and featuring a pronounced downward drag of strata in the food wall down block, implying a normal inversion at times.
Elbart Subfault
Elbart Nebenstörung
Gewellt, ingesamt N-S verlaufende Nebenstörung zwischen der Freihung Störung [DE-BY_990] im Westen und der Tanzfleck Störung [DE-BY_1390] im Osten.
Undulate, overall N-S trending subfault in between Freihung Fault [DE-BY_990] to the west and Tanzfleck Fault [DE-BY_1390] to the east.
Freihung Fault
Freihunger Störung
Freihunger Überschiebung
NNW-SSE verlaufende Hauptstörung der Freihunger Störungszone [DE-BY_1388]. Steil nach NE einfallende Aufschiebung mit einer Sprunghöhe von bis zu 1,2 km, mehrfach von Querstörungen versetzt.
NNW-SSE trending principal fault of Freihung Fault System [DE-BY_1388]. Steeply NE dipping reverse fault with a throw up to 1.2 km, repeatedly displaced by lateral faults.
Freihung cross-faults
Freihunger Querstörungen
SW-NE bis W-E streichende, saigere bis subvertikale Störungen die die Freihung Störung [DE-BY_990] und Elbart Nebenstörung [DE-BY_1389] versetzen und abschnittsweise zusammenführen.
SW-NE to W-E striking, vertical to subvertical faults displacing Freihung Fault [DE-BY_990] and Elbart Subfault [DE-BY_1389] and merging them in sections.
Kirchenthumbach-Pappenberg Fault Zone
Kirchenthumbach-Pappenberg Störungszone
Südliche Fortsetzung der Creußen Störung [DE-BY_961]. NNW-SSE streichendes Abschiebungssystem mit Einfallrichtung ENE, durch Querstörungen gegliedert
Southern continuation of Creussen Fault [DE-BY_961]. NNW-SSE trending normal fault system with dip direction ENE, structured by transverse faults.
Zissenhof-Pappenberg Fault
Zißenhof-Pappenberg- Störung
NNW-SSE verlaufende, steil nach NE einfallende Abschiebung mit einem Vertikalversatz von ca. 100 m.
NNW-SSE trending, steeply NE dipping normal fault featuring a throw of about 100 m.
Glosenrangen Cross Fault
Glosenrangen Querstörung
W-E bis SW-NE verlaufender Querbruch (Durchbruch) einer Akkommodationszone (breached relay ramp) im Überlappungsbereich der Zißenhof-Pappenberg Störung [DE-BY_1392] und Freihung Störung [DE-BY_990].
W-E to SW-NE trending connecting fault of a breached relay ramp as the overlap bridging between Freihung Fault [DE-BY_990] and Zissenhof-Pappenberg Fault [DE-BY_1392].
Weidenberg Fault
Weidenberg Störung
Weidenberger Störung
NW-SE streichende Ab- bzw. Steitenverschiebung mit Einfallrichtung NE
NW-SE trending normal/strike-slip fault with dip direction NE
Singenrain Fault
Singenrain Störung
N-S streichende Abschiebung mit Einfallrichtung W
N-S trending normal fault with dip direction W
Sesslach Fault
Sesslach Störung
NNW-SSE streichende Abschiebung mit Einfallrichtung ENE
NNW-SSE trending normal fault with dip direction ENE
Sennfeld-Weyer Fault Zone
Sennfeld-Weyer Störungszone
Seligenstadt-Brück Fault Zone
Seligenstadt-Brück Störungszone
Seifriedsburg Fault Zone
Seifriedsburg Störungszone
NW-SE streichende Abschiebung (Graben mit dextraler Seitenverschiebung? )
NW-SE trending normal fault (graben with dextral strike-slip?)
Hollfeld Fault Zone
Hollfelder Störungszone
NW-SE streichende Abschiebung mit Einfallrichtung SW (später revers invertiert), Nordost-Grenze der Frankenalb Furche.
NW-SE trending normal fault with dip direction SW (later reversly inverted), northeastern boundary of Frankenalb trough.
Schippacher Sprung
Schippach Fault
Schippach Störung
N-S streichende, steil nach W einfallende Abschiebung mit einer Sprunghöhe von ca. 220 m; Ostflanke des Schippacher Grabens.
N-S trending, steeply W dipping normal fault wit a throw of about 220 m; eastern flank of Schippach Graben.
Schippach Graben Western Flank
Schippacher Graben Westflanke
N-S trending, steeply E dipping normal fault wit a throw of about 150 m; western flank of Schippach Graben.
N-S streichende, steil nach E einfallende Abschiebung mit einer Sprunghöhe von ca. 150 m; Westflanke des Schippacher Grabens.
Heustreu Fault Zone
Heustreuer Störungszone
NW-SE streichende dextrale Seitenverschiebung
NW-SE trending dextral strike-slip fault
Rodach Fault
Rodach Störung
SW-NE streichende Abschiebung mit Einfallrichtung SE
SW-NE trending normal fault with dip direction SE
Eltersdorf-Röthenbach-Weigenhofen Fault
Eltersdorf-Röthenbach-Weigenhofen Störung
Insgesamt WNE-ESE verlaufende, steil nach NNE einfallende Abschiebung mit einer Sprunghöhe bis zu 40 m.
Overall WNW-ESE trending, steeply NNE dipping normal fault featuring a throw of up to 40 m.
Rodenbach-Duttenbrunn Fault Zone
Rodenbach-Duttenbrunn Störungszone
SW-NE streichende Abschiebung mit Einfallrichtung SE (Graben)
SW-NE trending normal fault with dip direction SE (graben)
Eschlipper Tal Fault
Eschlipper Tal Störung
Eisfeld-Kulmbach Fault Zone
Eisfeld-Kulmbach Störungszone
NW-SE streichende Seitenverschiebung mit Einfallrichtung NE (revers aufschiebend invertiert, max. Versatz von 900 m)
NW-SE trending strike-slip fault with dip direction NE (reversly inverted, max. displacement of 900 m)
Eisfeld-Kulmbach Fault Zone Segment 2
Eisfeld-Kulmbach Störungszone Segment 2
NW-SE streichende Aufschiebung mit Einfallrichtung NE (max. Versatz von 900 m)
NW-SE trending reverse fault with dip direction NE (max. displacement of 900 m)
Culmbacher Spalte
Eisfeld-Kulmbach Fault Zone Segment 1
Eisfeld-Kulmbach Störungszone Segment 1
NW-SE streichende Seitenverschiebung mit Einfallrichtung NE (revers invertiert)
NW-SE trending strike-slip fault with dip direction NE (reversly inverted)
Eichelsbach Fault
Eichelsbach Störung
WNW-ESE streichende Abschiebung mit Einfallrichtung SSW
WNW-ESE trending normal fault with dip direction SSW
Bamberg-Neuses Fault
Bamberg-Neuses Störung
NW-SE streichende dextrale Abschiebung mit Einfallrichtung NE
NW-SE trending normal or dextral strike slipe fault with dip direction NE
Regnitz Valley Fault
Regnitztal Störung
Gewellt N-S bis NNW-SSE verlaufende Abschiebung mit Einfallrichtung E
Undulate N-S to NNW-SSE trending normal fault with dip direction E
Pegnitz Fault
Pegnitz Störung
NW-SE streichende dextrale Steitenverschiebung
Pautzfeld Fault Zone
Pautzfeld Störungszone
N-S streichende Abschiebung mit Einfallrichtung N
N-S trending normal fault with dip direction N
Oberkatz Fault Zone
Oberkatz Störungszone
N-S streichende Abschiebung mit Einfallrichtung W (Graben)
N-S trending normal fault with dip direction W (graben)
Nordheim Fault
Nordheim Störung
Neuhütten Fault
Neuhütten Störung
Hafenprepach Fault
Hafenprepach Störung
Muggenbach Fault
Muggenbach Störung
N-S streichende Ab- bzw. Steitenverschiebung mit Einfallrichtung E
N-S trending normal/strike-slip fault with dip direction E
Grettstadt-Aschbach Fault Zone
Grettstadt-Aschbach Störungszone
NW-SE streichende Abschiebung mit Einfallrichtung SW (dextral seitenverschiebend?)
NW-SE trending normal fault with dip direction SW (dextral strike-slip?)
Motten Fault Zone
Motten Störungszone
NW-SE streichende Abschiebung (Graben)
NW-SE trending normal fault (graben)
Gräfenberg Fault
Gräfenberg Störung
Mönchberg Fault
Mönchberg Störung
SSW-NNE streichende sinistrale Steitenverschiebung mit Einfallrichtung WNW (100-320 m Versatz)
SSW-NNE trending sinistral strike-slip fault with dip direction WNW (100-320 m displacement)
Freiberg-Döringstadt Fault
Freiberg-Döringstadt Störung
Breitenbuch Fault Zone
Breitenbuch Störungszone
Bischofsheim Fault
Bischofsheim Störung
WNW-ESE streichende Abschiebung mit Einfallrichtung NNE
WNW-ESE trending normal fault with dip direction NNE
Bieber Fault
Bieber Störung
Baunachtal Fault
Baunachtal Störung
NNW-SSE streichende Abschiebung mit Einfallrichtung ENE (seitenverschiebend?)
NNW-SSE trending normal fault with dip direction ENE (strike-slip?)
Mitwitz Fault
Mitwitz Störung
NW-SE streichende Ab- oder Aufschiebung mit Einfallrichtung SW oder NE
NW-SE trending normal or reverse fault with dip direction SW or NE
Lindelbach-Erlach Fault Zone
Lindelbach-Erlach Störungszone
Lichtenfels Fault
Lichtenfels Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW (später zu Aufschiebung invertiert)
NW-SE trending normal fault with dip direction SW (later reversly inverted)
Leidersbach-Hobbach Fault
Leidersbach-Hobbach Störung
NNW-SSE streichende Abschiebung mit Einfallrichtung WSW
NNW-SSE trending normal fault with dip direction WSW
Laudenbach Fault
Laudenbach Störung
Kümmelberg Fault
Kümmelberg Störung
Kronach Fault
Kronach Störung
Kronacher Verwerfung
SW-NE streichende Abschiebung mit Einfallrichtung SE; versetzt die Leuschberg-Rennesberg Störungen [DE-BY_1477] und Letzenhof Störung [DE-BY_1430] ab und endet am Frankenwald-Randbruch [DE-BY_1431].
SW-NE trending normal fault with dip direction SE; offsets Leuschberg-Rennesberg Faults [DE-BY_1477] and Letzenhof Fault [DE-BY_1430] and truncated at Franconian Forest Scarp [DE-BY_1431].
Ehrenbach Fault
Ehrenbach Störung
Donnersdorf-Karbach Fault Zone
Donnersdorf-Karbach Störungszone
Kist-Fuchsstadt Fault Zone
Kist-Fuchsstadt Störungszone
NW-SE streichende Aufschiebung mit Einfallrichtung NE (invertierter Graben?)
NW-SE trending reverse fault with dip direction NE (inverted graben)
Creussen Fault
Creußen Störung
Coburg Fault
Coburg Störung
Brücklein Fault Zone
Brücklein Störungszone
Ahorntal-Anticline Fault
Ahorntal-Antikline Störung
SW-NE streichende sinistrale Seitenverschiebung
SW-NE trending sinistral strike-slip fault
Bamberg-Neuses Fault Zone
Bamberg-Neuses Störungszone
NW-SE streichende dextrale Ab- und Seitenverschiebung mit Einfallrichtung NE
NW-SE trending dextral normal fault with dip direction NE
Bad Brückenau graben faults
Bad Brückenauer Graben Störungen
NNW-SSE streichende Abschiebung
NNW-SSE trending normal fault
Baad Fault
Baad Störung
NW-SE streichende Abschiebung mit Einfallrichtung NW
NW-SE trending normal fault with dip direction NW
Auerbach Fault
Auerbach Störung
SSW-NNE streichende Abschiebung mit Einfallrichtung WNW
SSW-NNE trending normal fault with dip direction WNW
Atzhausen-Kleinlangheim Fault Zone
Atzhausen-Kleinlangheim Störungszone
Asslitz-Saas Fault
Asslitz-Saas Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW (Döllnitz-Jösleiner und Motschenbacher Störung, abschiebend einfallend nach SW, aufschiebend einfallend nach NE)
NW-SE trending normal fault with dip direction SW (Döllnitz-Jösleiner and Motschenbacher Fault, normal dip SW or reverse dip NE)
Ruppersdorf-Moratneustetten Fault
Ruppersdorf-Moratneustettener Störung
NW-SE (herzynisch) verlaufende, steil nach WSW einfallende Abschiebung mit einer Sprunghöhe bis zu ca. 40 m.
NNW-SSE trending, steeply WSW dipping normal fault with a vertical offset up to approx. 40 m.
Ballstadt Fault
Ballstädter Störung
WNW-ESE verlaufende, steil nach SSW einfallende Abschiebung mit einer Sprunghöhe bis über 30 m.
WNW-ESE striking, steeply SSW dipping normal fault with a vertical offset up to more than 30 m.
Elpersdorf Fault
Elpersdorfer Störung
NW-SE (herzynisch) verlaufende, steil nach SW einfallende Abschiebung mit einer Sprunghöhe bis zu 30 m.
NW-SE trending, steeply SW dipping normal fault with a vertical offset up to 30 m.
Tiefenthal Fault
Tiefenthaler Verwerfung
NW-SE trending, steeply SW dipping normal fault with a throw up to 30 m.
Oberbessenbach-Heimbuchenthal Fault
NW-SE trending, steeply SW dipping normal fault with a throw of up to 80 m.
Oberbessenbach-Heimbuchenthal Störung
Soden-Oberwintersbach Fault
NW-SE trending, steeply SW dipping normal fault with a throw of about 60 m.
Soden-Oberwintersbach Störung
Schöllesberg Fault
NW-SE striking, steeply SW dipping normal fault
Schöllesberg Störung
Pisamberg-Hofstetten Fault
NW-SE trending, steeply SW dipping normal fault featuring a throw of up to 80 m.
Pisamberg-Hofstetten Störung
Hofstettener Störung
Tepla-Barrandium Suture
Baden Baden-Nuremberg-Erbendorf Line
Baden Baden-Nürnberg-Erbendorf Linie
Tepla-Barrandium Sutur
Das Grundgebirge im südlichen und mittleren Deutschland ist Teil des variszischen Kollisionsorogens, das Kossmat (1927) in stratigraphisch-lithologisch-tektonische Zonen gliederte, von Nord nach Süd, Rhenoherzynikum, Saxothuringikum und Moldanubikum. Die Sutur zwischen dem Moldanubikum und dem Saxothuringikum wird von der Baden Baden-Nürnberg-Erbendorf Linie (Reinhold 2005) markiert, die zwischen dem Schwarzwald und der Böhmischen Masse, überdeckt von der mächtigen Abfolge permo-mesozoischer Sedimente des Süddeutschen Schichtstufenlandes, nirgends direkt nachgewiesen ist. Ihr Verlauf ist aus geophysikalischen Vermessungen und wenigen tiefen Bohrungen abgeleitet.
Kossmat (1927) subdivided the basement of the Variscan collision orogen in central and southern Germany in three stratigraphic-lithologic-tectonic zones, from north to south, Rhenohercynian, Saxothuringian, and Moldanubian Zones. In between the Black Forest in the west and the Bohemian Massif in the east the suture between the Saxothuringian and Moldanubian Zones, the Baden Baden-Nuremberg-Erbendorf Linie (Reinhold 2005), has not been evidenced directly as covered by a thick Permo-Mesozoic sedimentary sequence of the South German Scarpland. Its trend is inferred from geophysical surveys and few deep drillings.
Hainberg-Kirchhöhe Fault
NW-SE trending, steeply NE dipping normal fault.
Hainberg-Kirchhöhe Störung
Laufen-Autenberg Fault
NW-SE trending, steeply SW dipping normal fault featuring a throw of up to 50 m.
Laufen-Autenberg Störung
Kehlrein-Kreuzberg Verwerfung
Frommetsfelden Fault
Frommetsfeldener Verwerfung
NW-SE (herzynisch) verlaufende, steil nach SW einfallende Abschiebung mit einem Vertikalversatz bis zu 60 m.
NW-SE trending, steeply SW dipping normal fault with a vertical offset up to 60 m.
Frankenheim Fault Zone
Frankenheimer Störungszone
Schillingsfürster Verwerfung
Frankenheimer Verwerfung
NW-SE (herzynisch) verlaufende, steil nach SW einfallende Abschiebung mit einer Sprunghöhe bis zu 35 m.
NW-SE trending, steeply SW dipping normal fault with a vertical offset up to 35 m.
Kaltenbronn-Kaierberg-Lölldorf Fault
Kaltenbronn-Kaierberg-Lölldorfer Verwerfung
WSW-ENE verlaufende Gruppe verzweigter steil nach NNW einfallender Abschiebungen mit einer Sprunghöhe bis zu 30 m als Fortsetzung der baden-württembergischen Neckar-Jagst Furche, einer Scherzone, die die Baden Baden-Nürnberg-Erbendorf Line [DE-BY_1547] begleitet (Reinhold 2005).
WSW-ENE trending array of branched steeply NNW dipping normal faults featuring a throw up to 30 m. This fault zone forms the on strike continuation of Neckar-Jagst Trough on Baden-Württemberg territory in the east, a shear zone inferred to accompany Baden Baden-Nuremberg-Erbendorf Line [DE-BY_1547] (Reinhold 2005).
Edelsfeld-Irlbach Fault Zone
Edelsfeld-Irlbacher Störungszone
Insgesamt W-E bis WNW-ESE verlaufende, steil nach ± S einfallende Aufschiebungen mit einer Sprunghöhe bis 70 m.
Overall W-E to WNW-ESE trending, steeply ± S dipping reverse faults with a vertical displacement of up to 70 m.
Hainberg Cross-Fault
SW-NE striking fault offsetting Auhof-Hainberg Fault [DE-BY_1562] to the SW.
Hainberg Querstörung
Wagenmühle-Erlenbach Fault
NW-SE striking, steeply NE dipping normal fault featuring a throw of up to 65 m.
Wagenmühle-Erlenbach Störung
Erlenbach Störung
Altenbuch Fault
NNW-SSE to NW-SE trending, steeply ± NE dipping normal fault featuring a throw of up to 50 m.
Altenbuch Störung
Hanau-Seligenstadt Basin faults
Beneath the Lower Main Plain west of Spessart and north of Odenwald, overlapping the border between Hesse and Bavaria with only a minor part in the east on Bavarian territory, the Hanau-Seligenstadt Basin represents a low subsidence Cenozoic subbasin of the Upper Rhine Graben. It is dominated by N-S to NNW-SSE trending normal faults structuring the basin into several horsts and grabens.
Störungen der Hanau-Seligenstädter Senke
Ringheim-Eisenbach Fault
Intersecting Stockstadt-Gross-Umstadt Block, NNW-SSE trending, in the south veering to WNW-ESE along Mümling valley, vertical to steeply ± NE dipping normal fault.
Ringheim-Eisenbach Störung
Auhof-Hainberg Fault
Intersecting Stockstadt-Gross-Umstadt Block, NNW-SSE striking, steeply ENE dipping normal fault.
Auhof-Hainberg Störung
Kahl-Stockstadt Fault
NNW-SSE trending, steeply WSW dipping normal fault featuring a throw of up to 170 m. Southwestern boundary of Kleinwelzheim Horst towards Hanau-Seligenstadt Basin, continuing as ENE dipping Stockstadt-Obernburg Graben Western Flank [DE-BY_1565] in the south.
Kahl-Stockstadt Störung
Ubstadt-Walldürn Fault Zone
Ubstadt-Walldürn Störungszone
SW-NE streichende sinistrale Steitenverschiebung mit Einfallrichtung NW
SW-NE trending sinistral strike-slip fault with dip direction NW
Wöllriederhof-Biebelried Fault Zone
Wöllriederhof-Biebelried Störungszone
Woffendorf Fault
Woffendorf Störung
Wippfeld-Prichsenstadt Fault Zone
Wippfeld-Prichsenstadt Störungszone
NW-SE streichende dextrale Ab- und Seitenverschiebung mit Einfallrichtung SW
NW-SE trending dextral normal/strike-slip fault with dip direction SW
Wiesenttal Fault
Wiesenttal Störung
Weismain Fault
Weismain Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW (revers invertiert Einfallrichtung NE)
NW-SE trending normal fault with dip direction SW (reversly inverted dip NE)
Staffelberg Fault
Staffelberg Störung
Kissingen-Hassfurt Fault Zone
Kissingen-Hassfurt Störungszone
Allgemein NW-SE streichende Ab- und Seitenverschiebung mit Einfallrichtung NE, möglicherweise revers invertiert im NW und dominierender Abschliebungskomponente im SE Teil
Generally NW-SE trending dextral normal fault with dip direction NE, probably reversely inverted in the NW and dominating normal faulting behaviour in the SE part
Oerlenbach-Waldsachsen Fault
Oerlenbach-Waldsachsen Störung
Kissingen-Hassfurt Störungszone Segment 3
NW-SO streichende dextrale Ab- und Seitenverschiebung mit Einfallrichtung NE
Arnshausen-Wittersberg Fault
Arnshausen-Wittersberg Störung
Kissingen-Hassfurt Störungszone Segment 2
N-S streichende dextrale Schrägabschiebung mit Einfallrichtung E
N-S trending dextral oblique-slip normal fault with dip direction E
Stangenroth-Kissingen Fault
Stangenroth-Kissingen Störung
Kissingen-Hassfurt Störungszone Segment 1
NW-SO streichende dextrale Ab- und Seitenverschiebung mit Einfallrichtung NE (revers invertiert?)
NW-SE trending dextral normal fault with dip direction NE (reversly inverted?)
Wonfurt-Aurach Fault Zone
Wonfurt-Aurach Störungszone
Oberleichtersbach-Kissingen Fault Zone
Oberleichtersbach-Kissingen Störungszone
Kissingen-Hassfurt Störungszone Segment 5
Hassfurt-Bischberg Fault
Hassfurt-Bischberg Störung
Kissingen-Hassfurt Störungszone Segment 4
Kilianshof Fault
Kilianshof Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW (Graben)
NW-SE trending normal fault with dip direction SW (graben)
Kemnath-Waldeck Fault
E-W streichende Ab- bzw. Steitenverschiebung mit Einfallrichtung S
E-W trending normal/strike-slip fault with dip direction S
Kemnath-Waldeck Störung
Karlstadt-Würzburg-Kitzingen Fault Zone
Karlstadt-Würzburg-Kitzingen Störungszone
Itztal Fault
Itztal Störung
Trebgast Fault
Trebgast Störung
Sulzbach Syncline NE boundary
Sulzbacher Mulde NE Rand
Nordwest-Rand der Sulzbacher Mulde und der südlich anschließenden Kallmünzer Mulde (Frankenalb Mulde) gebildet von Aufschiebungen und einer Abschiebung (invertierte Aufschiebung?).
Northwestern margin of Sulzbach syncline and its southward transition to Kallmünz syncline (Frankenalb syncline) formed by reverse faults and normal (inverted reverse?) fault.
Amberg-Diebis-Thanheim Fault
Amberg-Diebis-Thanheim Störung
Von der Pfahl-Aufschiebung [DE-BY_1364] bei Krumbach nahe Amberg, westlich subparallel zur Fensterbach [DE-BY_1376] und Pittersberger [DE-BY_1374] Störung ziehende, NW-SE verlaufende, steil nach NE einfallende Abschiebung (invertierte Aufschiebung?) mit einem Vertikalversatz von bis zu 150 m, abschnittsweise wohl als Flexur (Nordost-Flanke des Ebermannsdorfer Sattels nach Meyer 2000). Im Süden bei stark abnehmender Sprunghöhe auf NE-SW umbiegend. Nordwest-Rand des Übergangsbereichs von der Sulzbacher zur Kallmünzer Mulde im SW zum Pittersberger Sattel im NE.
From Pfahl Reverse Fault [DE-BY_1364] at Krumbach near Amberg, paralleling the trends of Fensterbach [DE-BY_1376] and Pittersberg [DE-BY_1374] faults, NW-SE trending, steeply NE dipping normal fault (inverted reverse fault?) featuring a throw of up to 150 m, in parts arguably as a flexure (NE flank of Ebermannsdorf anticline after Meyer 2000). In its south veering to a NE-SW trend with decreasing throw. Northwestern margin of Sulzbach to Kallmünz syncline transition zone in the SW towards Pittersberg anticline in the NE.
Sulzbach-Amberg Fault
Sulzbach-Amberg Störung
Amberg-Sulzbacher Störungszone
NW-SE streichende Aufschiebung mit Einfallrichtung NE und einem Vertikalversatz bis zu 150 m.
NW-SE trending reverse fault with dip direction NE featuring a throw of up to 150 m.
Sulzbach Fault
Sulzbach Störung
Sulzbacher Störungszone
NW-SE streichende Aufschiebung mit Einfallrichtung NE und einen Vertikalversatz von bis zu 200 m.
NW-SE trending reverse fault with dip direction NE, featuring a throw of up to 200 m.
Strahlungen-Münnerstadt-Graben
Nördlich von Münnerstadt SW-NE, südlich davon N-S streichendes Abschiebungs-Paar (abschnittsweise Staffelbrüche), die einen auffälligen, geknickten Graben bilden.
North of Münnerstadt SW-NE, south of N-S striking pair normal faults (in sections step faults) forming a conspicuous kinked graben structure.
Anterior Spessart faults
The Anterior Spessart (Kristalliner Vorspessart) is the only place on Bavarian territory where the basement of the Mid-German Crystalline Rise (Mitteldeutsche Kristallinschwelle) emerges, the swell between the Saxothuringian and Rhenohercynian Zones interpreted an island arc. Two predominant structures characterize the basement: the SW-NE striking Variscan fold architecture and the NW-SE (Hercynian) striking late to post-Variscan faults, reactivated during Late Cretaceous and Tertiary generating up- and down faulted blocks (Saxonian brittle tectonics). Most faults, also those transecting the surrounding Buntsandstein-Spessart, more or less follow the Hercynian trend, predominant in the entire Bavarian Scarp Land.
Störungen im Kristallinen Vorspessart
Mittelgrund-Verwerfung
Waldaschaff Fault Zone
NW-SE trending normal faults with a steep dip direction SW; the southern branch, Mittelgrund Fault, running from Waldaschaff to Heimbuchenthal, features a throw of up to 85 m.
Waldaschaff Störungszone
Schimborn-Laufach Fault
Schimborn-Laufach Störung
Oberwald-Hohl Fault
Slightly arcuate NW-SE trending oblique-slip normal fault
Oberwald-Hohl Störung
Stempelhöhe-Goldbach Fault
Slightly undulate NW-SE trending oblique-slip normal fault
Stempelhöhe-Goldbach Störung
Bauersberg Fault
NW-SE trending oblique-slip normal fault featuring an offset of about 200 m.
Bauersberg Störung
Rubenberg-Bischlingsberg Fault
Slightly arcuate NW-SE trending, steeply SW dipping normal fault.
Rubenberg-Bischlingsberg Störung
Geiselbach-Vormwald Fault
NW-SE trending, steeply SW dipping minor offset sinistral normal oblique-slip fault.
Geiselbach-Vormwald Störung
Geiselbacher Sprung
Stetten Fault
Stetten Störung
NW-SE streichende Abschiebung mit Einfallrichtung SW (oder dextrale Seitenverschiebung?)
NW-SE trending normal fault with dip direction SW (or dextral strike-slip?)
Steinbach-Steinfeld-Retzbach Fault Zone
Steinbach-Steinfeld-Retzbach Störungszone
Staffelstein Fault Zone
Staffelstein Störungszone
NW-SE streichende Abschiebung mit Einfallrichtung NE, Südwestrand des Staffelsteiner Grabens.
NW-SE trending normal fault with dip direction NE, southwestern boundary of Staffelstein Graben.
3: Bohemian Massif domain
Grundgebirge der Böhmischen Masse
The tectonic boundary inventory within the verdant Bohemian Massif rock suites, apart from larger scale faults manifested in fractured zones and tectonites or evidence in scarce quarries, only rarely can be observed directly. Fault pattern are inferred mostly from indirect field evidence such as conspicuous lithological changes, joint system measurements, linear features like quartz veins, aligned with remote sensing data and geophysical surveys in few areas. By nature, these investigations do not allow for exact information on the dip angle and vertical displacement. Accordingly, the concepts’ statements on these parameters shall be considered an assumption. Small-scale faults and fractures of fragmented plutonic complexes (granite tectonics) are not considered.
Das Inventar tektonischer Grenzflächen in den Gesteinen der stark bewachsenen Böhmischen Masse, kann, mit Ausnahme größerer Störungszonen die sich in Zerrüttungszonen und dem Vorkommen von Tektoniten ausdrücken, sowie den Beobachtungen in Steinbrüchen, nur selten direkt eruiert werden. Die Störungsmuster sind daher meist aus indirekten Geländebefunden abgeleitet, wie abrupte Gesteinswechsel, Kluftmessungs-Diagrammen oder linearen Bildungen wie Quarzgängen, z. T. im Kontext mit Fernerkundungsdaten und geophysikalischen Untersuchungen in ausgesuchten Gebieten. Naturgemäß sind aus solchen Informationen keine genauen Aussagen zum Einfallswinkel und Sprunghöhe der Störungen zu treffen; die Angaben zu diesen Parametern in den Konzepten sind daher als Annahmen zu verstehen. Texturen und Kleinstrukturen fragmentierter Plutonit-Komplexe (Granittektonik) sind in den Konzepten nicht berücksichtigt.
Das Störungsmuster aller größeren stratigraphisch-lithologisch-tektonischen Einheiten der Böhmischen Masse in Bayern, Saxothuringikum, Moldanubikum und Münchberger Masse (eine Überschiebungsinsel des Teplá-Barrandiums), wird von grob NW-SE, flach herzynisch (100-120°) bis steil herzynisch (130-140°) verlaufenden Störungen oder Störungszonen dominiert. Diese bilden insbesondere im Moldanubikum großräumige polyphase Scherzonen, die teilweise bis weit in das permo-mesozoische Vorland reichen. Querstörungen, im Süden überwiegend ± N-S verlaufend, im Norden meist ± SW-NE, parallel zu den Suturen der variszischen Kollisionstektonik, ergänzen das Gesamtbild.
Overlapping the principal stratigraphic-lithologic-tectonic zones of the Bohemian Massif in Bavaria, Saxothuringian Zone, Moldanubian Zone and Münchberg Klippe (a Teplá-Barrandian thrust outlier), roughly NW-SE, flat-angle Hercynian (100-120°) to high-angle Hercynian (130-140°) trending faults or fault zones prevail the tectonic boundaries pattern, particularly in the Moldanubian Zone forming large-scale polyphase shear zones partially protruding into the Permo-mesozoic foreland. Transverse faults, predominantly ± N-S trending in the south, prevalently ± SW-NE in the north, resuming the orientation of accreted terranes sutures, complement the overall picture.
Erbendorf Line
Erbendorfer Linie
Östlich der Fränkischen Linie [DE-BY_1398], wo das variszische Grundgebirge zu Tage tritt, ist die Sutur zwischen dem niedrig metamorphen Saxothuringikum und dem hoch metamorphen Moldanubikum streckenweise aufgeschlossen, oft jedoch durch granitische Intrusionen ersetzt oder von jüngeren (tertiären) Sedimenten verdeckt. Im äußersten Westen und im Osten, wo sich die Struktur auf Tschechischen Territorium bis zur Westböhmischen Scherzone [DE-BY_1353] fortsetzt, markiert die Erbendorf Linie den Nordrand des Teplá-Barrandiums bzw. von Klippen sehr ähnlicher Lithologie (Zone von Erbendorf-Vohenstrauß).
East of the Franconian Line [DE-BY_1398] where the Variscan Basement emerges, the suture separating the high-grade metamorphic Moldanubian Zone to the south and the low-grade metamorphic Saxothuringian Zone to the north, the Baden Baden-Nuremberg-Erbendorf Line, subcrops in certain sections but is replaced by granitic intrusions or concealed by younger (Tertiary) deposits in large areas. In its very west and to the east, continuing on Czech territory to the West Bohemian Shear Zone [DE-BY_1353], Erbendorf Line marks the northern limit of the Teplá-Barrandian Zone or its outliers (Erbendorf-Vohenstrauss Zone).
Grötschenreuth-Siegritz Fault
Grötschenreuth-Siegritz Störung
Insgesamt W-E verlaufender Abschnitt der Erbendorfer Linie [DE-BY_1447] östlich der Fichtelnaab Störungszone [DE-BY_1451].
Overall W-E trending segment of Erbendorf Line [DE-BY_1447] east of Fichtelnaab Fault Zone [DE-BY_1451].
Hahneneggaten-Grötschenreuth Fault
Hahneneggaten-Grötschenreuth Störung
Westlichster Abschnitt der Erbendorfer Linie [DE-BY_1447], W-E streichende nördliche Grenze der Erbendorf-Vohenstrauß Zone [vgl. DE-BY_1451], einem isolierten Vorkommen (Klippe) des Teplá-Barrandiums.
Western section of Erbendorf Line [DE-BY_1447], W-E striking northern boundary of the Erbendorf-Vohenstrauss Zone [cf. DE-BY_1451], an outlier of the Teplá-Barrandian Terrane.
Pilmersreuth-Mähring Fault
Pilmersreuth-Mähring Störung
Insgesamt WSW-ENE verlaufende, saigere bis subvertikale Störung die der Erbendorfer Linie [DE-BY_1447] zugerechnet wird; mehrfach von den herzynischen Störungen des Stiftslands [DE-BY_1455] versetzt.
Overall WSW-ENE trending vertical to subvertical fault assigned to Erbendorf Line [DE-BY_1447], multiply offset by Stiftsland Hercynian faults [DE-BY_1455].
Leonberg-Wondreb Fault
Leonberg-Wondreb Störung
NW-SE verlaufende, saigere bis subvertikale Störung die die Erbendorfer Linie [DE-BY_1447] mehr als 10 km nach SE versetzt.
NW-SE trending vertical to subvertical fault offsetting Erbendorf Line [DE-BY_1447] by more than 10 km to the SE.
Mitterteich Graben boundaries
Mitterteich Grabenränder
Nach den unterschiedlichen Bohrtiefen der Basis der unverfestigten Tertiär-Ablagerungen des Mitterteicher Beckens, erscheint eine grabenartige Struktur in Grundgebirge gesichert. Der Verlauf der gegensinnig einfallenden Bruchstaffeln der Grabenflanken parallel zur Erbendorfer Linie [DE-BY_1447] jedoch ist angenommen, da Nachweise zur Verlaufsrichtung bisher fehlen.
Infrerred from the different depths of the base of Mitterteich Basin Tertiary unconsolidated deposits in various drillings, the existence of a graben-like structure is assured. However, the WSW-ENE trend of the inversely arranged step faults forming the flanks of the graben parallel to Erbendorf Line [DE-BY_1447] is assumed only as there is no evidence substantiating this orientation.
Wetzldorf Fault
Wetzldorf Störung
NW-SE streichende Querstörung zur Grötschenreuth-Siegritz Störung [DE-BY_1449].
NW-SE striking lateral fault of Grötschenreuth-Siegritz Fault [DE-BY_1449].
ZTM Southern Boundary
ZTM Südgrenze
Southern Boundary of the Tischenreuth-Mähring Zone (ZTM) an thrust outlier resembling the lithology of the Teplá-Barrandian Block, to the north bound by Erbendorf Line [LfU-BY_1447].
Moldanubian Zone tectonic boundaries
Tektonische Grenzflächen des Moldanubikums
Das Moldanubikum wird von spät-variszischen Blattverschiebungs-Bewegungen dominiert, die sich in NW-SE verlaufenden Scherzonen ausdrücken. Dementsprechend wird das Moldanubikum von grob NW-SE, flach herzynisch (100-120°) bis steil herzynisch (130-140°) streichenden, steilstehenden bis saigeren Störungen (sub-)parallel zu diesen Scherzonen charakterisiert und den kinematisch verbundenen, spitzwinklig dazu verlaufenden Nebenstörungen. Insbesondere der Bayerische Wald wird zudem von einer Vielzahl an mehr oder weniger N-S gerichteten Störungen durchsetzt. Der Ostrand der Bodenwöhrer Senke wird durch ein solches Störungsbündel begrenzt, das zu einem großen, sich nach Süden zur Stallwanger Furche fortsetzenden Störungssystem gehört. Östlich vom Cham, am Hohen Bogen, wurde die südwestliche Ausbuchtung des Teplá-Barrandiums in und auf das Moldanubikum s. str. geschoben und endet dort an einer bogenförmigen Scherzone aus invertierten Aufschiebungen.
Late Varican strike-slip faulting dominates the Moldanubian Zone, manifested in the extensive NW-SE trending shear zones. Accordingly, the Moldanubian Zone is characterized by roughly NW-SE, flat-angle Hercynian (100-120°) to high-angle Hercynian (130-140°) striking, subvertical to vertical faults (sub-)parallel to these shear zones and their acute-angled kinematically connected subsidiary faults. In addition, specifically the Bavarian Forest features a multitude of more or less N-S oriented faults. The eastern margin of Bodenwöhr Trough is bounded by a set of such faults, which are part of a major fault system continuing south to Stallwang Trench (Stallwanger Furche). East of Cham, the southwestern bulge of the Teplá-Barrandian Terrane is thrusted into the Moldanubian s. str., manifested in a bow-shaped shear zone system of inverted thrust faults.
Weisser Regen Fault
Weißer Regen Störung
Im östlichen Lamer Winkel entlang des Weißen Regens, leicht gewellt NW-SE verlaufende, saigere bis subvertikale Blattverschiebung grob parallel zur Rundinger Zone [DE-BY_1348].
Following Weisser Regen river valley in the east of Lamer Winkel, slightly undulate NW-SE trending vertical to subvertical strike-slip fault roughly parallel to Runding Zone [DE-BY_1348].
Nottersdorf Fault Zone
Nottersdorf Störungszone
NNW-SSE streichende, steil nach ENE einfallende Aufschiebung, entsprechend dem Versatz von Markerzonen (Wagner et al. 1997) mit einem Vertikalversatz von ca. 1,8 km.
NNW-SSE striking, steeply ENE dipping reverse fault, according to the vertical displacement of marker horizons (Wagner et al. 1997) featuring a vertical offset of about 1.8 km.
Fichtelnaab lateral faults
Fichtelnaab Quer-Störungen
Schar SW-NE streichender, saigerer bis subvertikaler Störungen die rechtwinklig bis stumpfwinklig zur Fichtelnaab Störungstone [DE-BY_1451] verlaufen.
Set of SW-NE striking, vertical to subvertical faults trending perpendicular to obtuse-angled to Fichtelnaab Fault Zone [DE-BY_1451].
Fichtelnaab Fault Zone
Fichtelnaab Störungszone
Fichtelnaab Fault
SE4 (Seismic Event 4)
Fichtelnaab Störung
Seismischer Reflektor SE3
NW-SE to W-E trending, steeply to intermediately NE to N dipping major tectonic structure branching off and kinematically related to Franconian Line [DE-BY_1398] with a (cumulative) vertical displacement of about 1.7 km (Wagner et al. 1997). Main development phases have been late Variscan NE-SW compression, dextral movement during Early Cretaceous, and the uplift of the Variscan Basement and the overthrust of the foreland during Late Cretaceous and Paleogene (Zulauf 1991). In its northern part eastern boundary of the Zone of Erbendorf-Vohenstrauss (ZEV) featuring a composition very much resembling the lithological units of the Teplá-Barrandian Terrane, thus considered an outlier of the “Bohemicum”, to the west bound by Franconian Line [DE-BY_1398] and in the south reaching to Luhe Fault [DE-BY_965].
NW-SW bis W-E verlaufende, steil bis mäßig steil nach NE bis N einfallende Großstruktur die von der Fränkischen Linie [DE-BY_1398] abzweigt, mit dieser kinematisch verbunden ist und nach Markerzonen (Wagner et al. 1997) einen (kumulativen) Vertikalversatz von etwa 1,7 km aufweist. Haupt-Entstehungsphasen waren nach Zulauf (1991): Anlage während der postvarizischen NE-SW Kompression, dextrale Bewegungen während der N-S Kompression in der Unterkreide, Aufschiebung und Hebung des Grundgebirges auf das Vorland während der alpidischen Gebirgsbildung (Oberkreide bis Paläogen). Östliche Begrenzung der Zone von Erbendorf-Vohenstrauß (ZEV), die kompositionell stark den lithologischen Einheiten des Teplá-Barrandiums gleicht und daher als Überschiebungsklippe des "Bohemikum" angesehen wird, die sich im Süden bis zur Luhe Störung [DE-BY_965] erstreckt und im Westen von der Fränkischen Linie [DE-BY_1398] begrenzt wird.
Runding Zone
Rundinger Zone
Von Pempfling NW von Cham, verzweigt in zwei Teiläste nach Langdorf und Regen, über ca. 50 km ziehende, NW-SE verlaufende, steil nach NE einfallende spätvariszische mylonitische Scherzone parallel zur Pfahl Scherzone [DE-BY_1362] (Regen Ast: parallel zum NNW-SSE Trend der Rattenberg Zone [DE-BY_1349]). Diese Scherzone wird von späteren vertikalen Störungen und Mineralgängen gekreuzt, weist aber keinen hydrothermalen Gangquarz im Streichen auf.
Running for about 50 km from Pempfling NW of Cham, branched in two tail ends to Langdorf and Regen. This overall NW-SE trending steeply NE dipping Late Varican mylonitic shear zone parallel to Pfahl Shear Zone [DE-BY_1362] (Regen branch: paralleling the NNW-SSE trend of Rattenberg Zone [DE-BY_1349]) is intersected by later vertical faults and mineral veins but does not feature hydrothermal vein quartz along the strike.
Runding Zone extension faults
Rundinger Zone Längsstörungen
Grob NW-SE verlaufende, saigere bis subvertikale Störungen die die Hauptstreichrichtung der Rundiger Zone nach SE hin fortsetzen.
Roughly NW-SE trending vertical to subvertical faults sustaining the principal strike direction of Runding Zone to the southeast.
Runding Zone Lateral Faults
Rundinger Zone Querstörungen
Saigere bis subvertikale Störungen senkrecht zum Streichen der Rundinger Zone verlaufen.
Vertical to subvertical faults trending perpendicular to the strike of Runding Zone.
Runding Zone Subsidiary Faults
Rundinger Zone Nebenstörungen
Saigere bis subvertikale Störungen die subparallel bis spitzwinklig zum Streichen der Rundinger Zone verlaufen.
Vertical to subvertical faults trending subparallel or acute-angled to the strike of Runding Zone.
Runding Zone Horsetail Splay
Rundinger Zone Wedel
Gleich wie die Abteiland Diagonal Störungen [DE-BY_1416] für die Pfahl Scherzone werden diese kleinräumigen, saigeren bis sub-vertikalen Störungen östlich von Zwiesel, die radialstrahlig SSW-NNE bis WNW-ESE verlaufen, als "Pferdeschwanz"-Auffiederungen (horsetail splays) der Rundinger Zone [DE-BY_1348] interpretiert (Eberts et al. 2021).
Likewise Abteiland Diagonal Faults [DE-BY_1416] for the Pfahl Shear Zone, these small-scale vertical to subvertical faults east of Zwiesel, trending radially SSW-NNE to WNW-ESE, are interpreted horsetail splays (Eberts et al. 2021) of Runding Zone [DE-BY_1348].
Waldthurn-Vohenstrauss Fault
Waldthurn-Vohenstrauß Störung
Zwischen Ellenbach und Kößing verfolgbare Ostgrenze der Zone von Erbendorf-Vohenstrauß (ZEV), einer Überschiebungsinsel der Teplá-Barrandium Domäne. Insgesamt N-S verlaufende, saigere bis subvertikale Störung, deren geknickter NNW-SSE und NNE-SSW Verlauf in Abschnitten dem Trend der Herzynische Strukturen des Oberpfälzer Waldes [DE-BY_1454] folgt. Verbindung zwischen der Luhe Störung [DE-BY_965] und der Cham Störung [DE-BY_1408].
Traceable between Ellenbach and Kössing eastern boundary of Erbendorf-Vohenstrauss Zone (ZEV), an outlier of Teplá-Barrandian domain. Overall N-S trending, vertical to subvertical fault. Its kinked NNW-SSE and NNE-SSW trend in segments resumes the strike of the Upper Palatine Forest Hercynian structures [DE-BY_1454]. Link between Luhe Fault [DE-BY_965] and Cham Fault [DE-BY_1408].
Upper Palatine Forest Hercynian structures
Herzynische Strukturen des Oberpfälzer Waldes
Flach herzynisch (100-120°) streichende, saigere bis subvertikale Störungen und Quarzgänge, ± parallel zur Westböhmischen Scherzone [DE-BY_1353] auf tschechischem Gebiet.
Flat-angle Hercynian (100-120°) striking, vertical to subvertical faults and quartz veins, more or less paralleling West Bohemian Shear Zone [DE-BY_1353] on Czech territory.
Waldmünchen-Gleissenberg Fault
Waldmünchen-Gleißenberg Störung
NNW-SSE streichende Hauptstörung mit einer NNE-SSW verlaufenden Zweigstörung in der Überganszone der Bayerwald Meridional Störungen [DE-BY_1350] zu den herzynischen Strukturen des Oberpfälzer Waldes [DE-BY_1454]. Die Hauptstörung übernimmt dabei den Trend der herzynischen Strukturen des Oberpfälzer Waldes [DE-BY_1454], mehr oder weniger parallel zum Verlauf der Westböhmischen Scherzone [DE-BY_1353] auf tschechischem Gebiet.
NNW-SSE striking main fault with a NNE-SSW trending branch overlapping the transition zone of Bayerwald Meridional Faults [DE-BY_1350] and Upper Palatine Forest Hercynian structures [DE-BY_1454]. The main fault adopts the strike of Upper Palatine Forest Hercynian structures [DE-BY_1454], more or less paralleling West Bohemian Shear Zone [DE-BY_1353] on Czech territory.
Waldmünchen Faults
Waldmünchen Störungen
Schar NNW-SSE bis NW-SE verlaufender, ± vertikaler Störungen in der Überganszone der Bayerwald Meridional Störungen [DE-BY_1350] zu den herzynischen Strukturen des Oberpfälzer Waldes [DE-BY_1454].
Array of NNW-SSE to NW-SE trending ± vertical faults in the transition zone of Bayerwald Meridional Faults [DE-BY_1350] and Upper Palatine Forest Hercynian structures [DE-BY_1454].
Tiefenbach-Treffelstein Fault
Tiefenbach-Treffelstein Störung
NW-SE streichende, saigere bis subvertikale Störung in der Überganszone der Bayerwald Meridional Störungen [DE-BY_1350] zu den herzynischen Strukturen des Oberpfälzer Waldes [DE-BY_1454].
NW-SE striking vertical to subvertical fault in the transition zone of Bayerwald Meridional Faults [DE-BY_1350] and Upper Palatine Forest Hercynian structures [DE-BY_1454].
Bayerwald Meridional Faults
Bayerwald Meridional Störungen
Überwiegend aus dem Verlauf von Tälern abgeleitet, im km-Bereich weitständig subparallel, übergeordnet N-S (NNW-SSE bis NNE-SSW) verlaufende Störungsschar steil einfallender bis saigerer Störungen vorwiegend im Vorderen Bayerischen Wald. Diese stumpfwinklig zur Pfahl Scherzone [DE-BY_1362] und Rundinger Zone [DE-BY_1348] verlaufenden Scherbrüche können als R‘- oder P'-Riedelbrüche interpretiert werden, die während der frühen Stadien der Scherung angelegt werden, aber sich dabei nicht weit fortpflanzen, als präexistente Klüfte bei einer späteren Reaktivierung aber vergrößert und verlängert wurden. Bedingt durch die spät- bis postvariszische bruchhaft-spröde Deformation und Hebung, und deren Reaktivierung während der Unterkreide und im Alttertiär als Fernwirkung der alpinen Gebirgsbildung, wird das Terrain schollenartig zerlegt (Teipel et al. 2013) und die tertiäre Talbildung vorgezeichnet.
Mostly inferred from the conspicuous trend of valleys, array of subparallel, km-spaced, overall N-S (NNW-SSE to NNE-SSW) trending, steeply dipping to vertical faults predominantly transecting the Anterior Bavarian Forest aka Danube Hills. These faults, obtuse angled with respect to the Pfahl Shear Zone [DE-BY_1362] and Runding Zone [DE-BY_1348] may be interpreted R’- or P'-Riedel shears, i.e. subsidiary shear fractures accommodating strain in the fault zone, coeval with the main wrench faulting and propagating a short distance out it, however enlarged and extended during later reactivation. This late to post-Variscan brittle deformation and the uplift of the terrain led to a slab-like fragmentation, reactivated during Late Cretaceous and Paleogene as a distant effect of the Alpine orogenesis, and predetermined the Tertiary valley formation (Teipel et al. 2013).
N-S bis NNW-SSE verlaufender Störungszug steil einfallender bis saigerer Bayerwald Meridional Störungen zwischen Kollnburg nahe der Pfahl Scherzone [DE-BY_1362] und dem Donaurandbruch [DE-BY_698] südlich von Schwarzach. Die südlichen Abschnitte bilden den Ostrand der Stallwanger Furche.
Kollnburg-Schwarzach Fault
Kollnburg-Schwarzach Störung
Linear array of N-S to NNW-SSE trending steeply dipping to vertical Bayerwald Meridional Faults between Kollnburg close to the Pfahl Shear Zone [DE-BY_1362] and Donaurand Fault Scarp [DE-BY_698] south of Schwarzach. Southern sections form the eastern boundary of Stallwang Trench (Stallwanger Furche).
Running from Hunderdorf to Danube river, NNW-SSE striking steeply dipping to vertical dextral oblique-slip fault slightly displacing the Danube Fault Scarp [DE-BY_698] and Steinach-Deggendorf Fault [DE-BY_1538].
Von Hunderdorf zur Donau verlaufende, NNW-SSE streichende, steil einfallende bis saigere, rechtssinnige Querverschiebung, die den Donaurandbruch [DE-BY_698] und die Steinach-Deggendorf Fault [DE-BY_1538] leicht versetzt.
Hunderdorf Fault
Hunderdorf Störung
Teisnach-Deggendorf Fault
Teisnach-Deggendorf Störung
Von Asbach nördlich von Teisnach, über die Pfahl Scherzone [DE-BY_1362] bis nach Deggendorf verlaufender, längster und auffälligster Vertreter der Bayerwald Meridional Störungen. Setzt sich, im Kollbachtal verschoben, SSE-wärts bis in das randliche Molassebecken fort, wo die Störung den Donaurandbruch [DE-BY_698] leicht versetzt.
The longest and most conspicuous member of the Bayerwald Meridional Fault running from Asbach north of Teisnach, crossing Pfahl Shear Zone [DE-BY_1362] at Pattersdorf, to Deggendorf and, offset in Kollbach Valley, further into the marginal Molasse Basin thereby slightly displacing the Danube Fault Scarp [DE-BY_698].
Kittenrain Faults
Kittenrain Störungen
Subparalleles Paar NW-SW verlaufender, saigerer bis subvertikaler Störungen überwiegend als Quarz (+ Flußspat) Gänge, im Süden vom Donaurandbruch [DE-BY_698] begrenzt.
Subparallel pair of NW-SW trending, vertical to subvertical faults predominantly manifested in quartz (+ fluorite) veins, in the south truncated by Donaurand Fault Scarp [DE-BY_698].
Falkensteiner Vorwald Faults
Falkensteiner Vorwald Störungen
Der Falkensteiner Vorwald, der westlichste Ausläufer des Bayerischen Waldes, wird von plutonischer Kleintektonik der karbonischen Granit-Komplexe dominiert. Neben diesen kleinräumigen Texturen treten nur wenige ± vertikale Störungen, ohne vorherrschende Streichrichtung auf. Demgegenüber zeigen die post-granitischen Gänge, die im Westteil des Falkensteiner Vorwalds gehäuft auftreten, eine bevorzugte Orientierung subparallel zum Keilberg Störungssystem [DE-BY_1484] und den Bayerwald Meridional Störungen [DE-BY_1350].
The Falkensteiner Vorwald (Falkenstein Anterior Forest), the westernmost foothills of the Bavarian Forest, is dominated by primary features of the Carboniferous granite batholith complexes. Beyond these small-scale textures only few ± vertical faults occur featuring no predominant strike direction. The post-granitic dykes accumulating in the western part of Falkensteiner Vorwald, however, show a preferred orientation subparallel to Keilberg Fault System [DE-BY_1484] and the Bayerwald Meridional Faults [DE-BY_1350].
NNW-SSE trending, vertical to steeply WSW dipping Late Variscan mylonitic shear zone running from Dietersdorf to Haigrub; eastern boundary of Stallwang Trench (Stallwanger Furche).
Rattenberg Zone
Rattenberger Zone
NNW-SSE verlaufende, saigere bis steil nach WSW einfallende spätvariszische mylonitische Scherzone zwischen Dietersdorf und Haigrub; Ostrand der Stallwanger Furche.
Rattenberg-Haselbach Fault
Rattenberg-Haselbach Störung
N-S bis NNE-SSW verlaufende, saigere bis steil einfallende Störung; vermuteter Ostrand der Stallwanger Furche.
N-S to NNE-SSW trending, vertical to steeply dipping fault; assumed eastern boundary of Stallwang Trench (Stallwanger Furche).
St. Englmar Fault
St. Englmar Störung
NNW-SSE streichende, saigere bis steil einfallende Störung, im Nordteil mit der Rattenberger Zone [DE-BY_1349] zusammenlaufend, im Südteil parallel zum südlichen Ausläufer dieser mylonitischen Scherzone.
NNW-SSE striking, vertical to steeply dipping fault converging with Rattenberg Zone [DE-BY_1349] in the north and paralleling the southern tail of this mylonitic shear zone in the south.
Slightly arcuate N-S to NNW-SSE trending, vertical to steeply dipping fault, in its northern part truncating Rattenberg Zone [DE-BY_1349], in its southern part paralleling this mylonitic shear zone. Assumed eastern boundary of Stallwang Trench (Stallwanger Furche).
Dietersdorf Fault
Dietersdorf Störung
Leicht gebogen N-S bis NNW-SSE verlaufende, saigere bis steil einfallende Störung, im Nordteil Begrenzung der Rattenberger Zone [DE-BY_1349], im Südteil parallel zu dieser mylonitischen Scherzone. Vermuteter Ostrand der Stallwanger Furche.
Schwaighof-Momansfelden Störung
Schwaighof-Momansfelden Fault
NW-SE verlaufende, steil nach NE einfallende Intra-Grundgebirge Störung, wahrscheinlich Aufschiebung.
NW-SE trending, steeply NE dipping intra-basement fault, probably reverse fault.
Trasching-Michelsneukirchen Faults
Trasching-Michelsneukirchen Störungen
Am Südwest-Rand der Bodenwöhrer Senke parallel zur Nordrand-Störung, dem Pfahl Überschiebungssystem [DE-BY_ 1363], ziehende Störungen, die Grundgebirgs-Schollen auf die randlichen Kreide-Ablagerungen der Bödenwöhrer Senke aufschieben. Grob NW-SE bis WNW-ESE verlaufende, mäßig steil nach NE einfallende Auf- bzw. Überschiebungen mit einen (Residual-) Versatz von etwa 100 m.
Forming the southwestern margin of Bodenwöhr Through with the same orientation as the northern margin Pfahl Reverse Fault System [DE-BY_ 1363], roughly NW-SE to WNW-ESE trending, moderately NE dipping reverse resp. thrust faults with a (residual) displacement of about 100 m, thrusting basement blocks onto the marginal Cretaceous deposits of Bodenwöhr Trough.
Cham Fault
Cham Störung
Cham Fault System
Cham Störungssystem
NNW-SSE streichende tektonische Struktur krustalen Ausmaßes, die von nahe der Luhe Störung [DE-BY_965], im nördlichen Abschnitt parallel zur Westböhmischen Scherzone [DE-BY_1353] auf tschechischem Gebiet, den Bayerischen Pfahl [DE-BY_1347] bei Cham querend, bis zum Donaurandbruch [DE-BY_698] verläuft. Aus den Grenzlinien benachbarter Domänen unterschiedlicher Lithologie (Metamorphosegrad) abgeleitet, äußert sich diese bedeutende tektonische Struktur in diskontinuierlichen Segmenten aufgeschlossener Störungen oder Quarzgänge.
NNW-SSE trending tectonic structure of crustal extend, running from close to Luhe Fault [DE-BY_965], in its northern part paralleling West Bohemian Shear Zone [DE-BY_1353] on Czech territory, across the Bavarian Pfahl [DE-BY_1347] near Cham to Donaurand Fault Scarp [DE-BY_698]. Inferred from the borderlines of juxtaposed contrasting lithological (metamorphic grade) domains this major tectonic structure is manifests itself in discontinuous exposed fault segments and quartz veins.
Mitterfels-Bogen Störung
Mitterfels-Bogen Fault
Südlichstes Ost-Segment der Cham Störung [DE-BY_1408], als eine der größeren Bayerwald Meridional Störungen [DE-BY_1350]. N-S bis NNW-SSE verlaufende, steil bis senkrecht stehende rechtssinnige Schrägverschiebung die die Münster Graben Störung [DE-BY_1485] abschneidet und die Steinach-Deggendorf Störung [DE-BY_1538] sowie den Donaurandbruch [DE-BY_698] versetzt.
Major Bayerwald Meridional Fault [DE-BY_1350] forming the southernmost eastern segment of Cham Fault [DE-BY_1408] . N-S to NNW-SSE trending, steeply dipping to vertical dextral oblique-slip fault truncating Münster Graben Fault [DE-BY_1485] and displacing Steinach-Deggendorf Fault [DE-BY_1538] as well as Donaurand Fault Scarp [DE-BY_698].
Ascha-Furth Fault
Ascha-Furth Störung
Südlichstes West-Segment der Cham Störung [DE-BY_1408], als eine der größeren Bayerwald Meridional Störungen [DE-BY_1350]. N-S bis NNW-SSE verlaufende, steil nach NE bis ENE einfallende bis senkrecht stehende rechtssinnige Schrägverschiebung die die Münster Störung [DE-BY_1539] abschneidet und die Steinach-Deggendorf Störung [DE-BY_1538] sowie den Donaurandbruch [DE-BY_698] versetzt. Westliche Grenze der Stallwanger Furche.
Southernmost western segment of Cham Fault [DE-BY_1408] and a major Bayerwald Meridional Fault [DE-BY_1350]. N-S to NNW-SSE trending, steeply E to ENE dipping to vertical dextral oblique-slip fault truncating Münster Fault [DE-BY_1539] and displacing Steinach-Deggendorf Fault [DE-BY_1538] as well as Donaurand Fault Scarp [DE-BY_698]. Western boundary of Stallwang Trench (Stallwanger Furche).
Section of Cham Fault [DE-BY_1408] south of merger with Trasching-Michelsneukirchen Faults [DE-BY_1478] and western boundary of Stallwang Trench (Stallwanger Furche) as inferred by Eberts et al. (2021). Slightly undulate NNW-SSE trending, steeply ENE dipping to vertical normal fault, in sections manifested in quartz veins. Southern continuation of Wetterfeld-Höhhof Fault [DE-BY_1479], the structured Bodenwöhr Trough eastern boundary.
Höhhof-Rattiszell Fault
Höhhof-Rattiszell Störung
Abschnitt der Cham Störung [DE-BY_1408] südlich ihrer Verschmelzung mit den Trasching-Michelsneukirchen Störungen [DE-BY_1478] und der westlichen Begrenzung der Stallwanger Furche nach Eberts et al. (2021). Leicht gewellt NNW-SSE verlaufende, steil nach ENE einfallende bis senkrecht stehende Störung, abschnittsweise von Quarz-Gängen vertreten. Südliche Fortsetzung der Wetterfeld-Höhhof Fault [DE-BY_1479], als strukturiertem Ostrand der Bodenwöhrer Senke.
Wetterfeld-Höhhof Fault
Wetterfeld-Höhhof Störung
Abschnitt des West-Astes der Cham Störung [DE-BY_1408] als Ostgrenze der Bödenwöhrer Senke und von Eberts et al. (2021) abgeleitete westliche Begrenzung der Stallwanger Furche. Insgesamt NNW-SSE verlaufende, steil nach ENE einfallende bis saigere Abschiebung, abschnittsweise in zwei Äste aufgespalten und von Querstörungen versetzt. Setzt sich im Süden als Höhhof-Rattiszell Störung [DE-BY_1360] fort.
Section of the western branch of Cham Fault [DE-BY_1408] representing the structured Bodenwöhr Trough eastern boundary and the inferred western boundary of Stallwang Trench (Stallwanger Furche) (Eberts et al. 2021). Overall NNW-SSE trending, steeply ENE dipping to vertical normal fault in sections split up in two branches and displaced by lateral faults. Continues as Höhhof-Rattiszell Fault [DE-BY_1360] in the south.
Bernried-Rattiszell Fault
Bernried-Rattiszell Störung
Östlicher Ast der Cham Störung [DE-BY_1408], im Norden über den Kleine(i)nzenrieder Nebenpfahl (Dorn 1936) mit dem West-Ast verbunden. Leicht gewellt N-S bis NNW-SSE verlaufende, diskontinuierliche und abschnittsweise von Quarz-Gängen vertretene, steil bis senkrecht stehende Störung, die die Pfahl Scherzone DE-BY_1362] im Regental westlich von Cham kreuzt. Im südlichen Abschnitt verläuft die Störung östlich subparallel zum strukturierten Ostrand der Bodenwöhrer Senke und der damit verbundenen Höhhof-Rattiszell Störung [DE-BY_1360].
Eastern branch of Cham Fault [DE-BY_1408], in the north merging with the western branch via Kleinenzenrieder Nebenpfahl (Dorn 1936). Slightly undulate N-S to NNW-SSE trending, discontinuous and in sections manifested in quartz veins, steeply dipping to vertical fault crossing Pfahl Shear Zone [DE-BY_1362] in the Regen river valley west of Cham. In its southern section running easterly subparallel to the structured Bodenwöhr Trough eastern boundary and linked Höhhof-Rattiszell Fault [DE-BY_1360].
Stamsried Fault
Stamsried Störung
NNW-SSE verlaufendes, saiger bis steilstehendes Störungssegment des westlichen Astes der Cham Störung [DE-BY_1408]. Südliche Fortsetzung der Rötz-Großenzenried Störung [DE-BY_1412].
NNW-SSE trending, vertical to subvertical fault segment of Cham Fault [DE-BY_1408] western branch. Southern continuation of Rötz-Grossenzenried Fault [DE-BY_1412].
Rötz-Grossenzenried Fault
Rötz-Großenzenried Störung
N-S verlaufender nördlicher Teil des westlichen Astes der Cham Störung [DE-BY_1408]. Läuft im Norden mit dem Kleine(i)nzenrieder Nebenpfahl (Dorn 1936) zusammen, der nördlichen Fortsetzung der Bernried-Rattiszell Störung [DE-BY_1357] als östlichem Ast der Cham Störung.
N-S trending northern part of the western branch of Cham Fault [DE-BY_1408]. To the north merging with Kleinenzenrieder Nebenpfahl (Dorn 1936), the northern continuation of Bernried-Rattiszell Fault [DE-BY_1357] representing the Cham Fault Zone eastern branch.
Thanstein Fault
Thanstein Störung
NNW-SSE verlaufendes, saiger bis steilstehendes Störungssegment der Cham Störung [DE-BY_1408].
NNW-SSE trending, vertical to subvertical fault segment of Cham Fault [DE-BY_1408].
Pullenried-Winklarn dike swarm
Pullenried-Winklarn Gangschar
Abfolge steil herzynisch (130-140°) bis NNW-SSE streichender, saigerer bis steilstehender Quarzgänge und kurzer Störungssegmente parallel zu den Herzynische Strukturen des Oberpfälzer Waldes [DE-BY_1454 im Norden und zu den Bayerwald Meridional Störungen [DE-BY_1350] im Süden.
Succession of high-angle Hercynian (130-140°) to NNW-SSE striking, vertical to subvertical quartz veins and short fault segments, paralleling the Upper Palatine Forest Hercynian structures [DE-BY_1454] in the north and the Bayerwald Meridional Faults [DE-BY_1350] in the south.
Obertresenfeld-Braunetsrieth dike swarm
Obertresenfeld-Braunetsrieth Gangschar
Abfolge steil herzynisch (130-140°) streichender, saigerer bis steilstehender Quarzgänge und kurzer Störungssegmente parallel zu und Teil der Herzynische Strukturen des Oberpfälzer Waldes [DE-BY_1454].
Succession of high-angle Hercynian (130-140°) striking, vertical to subvertical quartz veins and short fault segments, parallel to and part of the Upper Palatine Forest Hercynian structures [DE-BY_1454].
Kemnath Fault
Kemnather Störung
NNW-SSE verlaufende Störung, die im nördlichen Abschnitt Trias (im W) gegen Grundgebirge (im E) versetzt, im südlichen Teil im Grundgebirge verläuft.
NNW-SSE trending fault, in its northern part offsetting Triassic deposits in the west towards the Variscan basement in the east, intra-basement in its southern part.
Falkenstein-Frauenau Fault
Falkenstein-Frauenau Störung
Leicht gebogen N-S bis NNW-SSE verlaufende steilstehende bis saigere Störung.
Slightly arcuate N-S to NNW-SSE trending steeply dipping to vertical fault.
Stockbach Fault
Stockbach Störung
N-S streichende Störung westlich von Nabburg.
N-S striking fault west of Nabburg.
Bavarian Pfahl
Bayerischer Pfahl
Von Amberg bis zur österreichischen Grenze nordöstlich von Passau und weiter zum Rodl-Kaplice Störungssystem südlich von Oberneukirchen (Oberösterreich) verlaufende, NW-SE streichende, mehr als 200 km lange spätvariszische Scherzone mit spröd-plastischer Deformation. Entstanden durch Krustendehnung mit Seitenverschiebungskomponente, überwiegend dextral, phasenweise sinistral, zeigt der großräumig als Mylonit ausgebildete südöstliche Abschnitt, die Pfahl Scherzone [DE-BY_1362], eine bruchhaft-spröde Reaktivierung mit der Bildung hydrothermaler Quarzgänge. Während der Heraushebung des Westrandes der Böhmischen Masse, als Fernwirkung der alpinen Gebirgsbildung in der Unterkreide und im Alttertiär, wirkte der nordwestliche Abschnitt, das Pfahl Aufschiebungssystem [DE-BY_1363], als Aufschiebungsfläche des Grundgebirges auf das permo-mesozoische Vorland. Hierdurch entstand die Bodenwöhrer Senke.
Running from Amberg to the Austrian border NE of Passau and beyond to Rodl-Kaplice Fault System south of Oberneukirchen (Upper Austria), this NW-SE striking, more than 200 km long Late Varican shear zone, is associated with brittle-ductile deformation. Initially subject to rift- and wrench-tectonic with a predominantly dextral, in phases sinistral shearing, the large-scale mylonitic southeastern section, the Pfahl Shear Zone [DE-BY_1362], shows a conspicuous later hydrothermal quartz mineralization forming the nearly vertical zones of Pfahl quartz along the strike. On uplift of the western margins of the Bohemian Massif, as a distant effect of the Alpine orogenesis during Late Cretaceous and Paleogene, particularly in its northwestern section, the Pfahl Reverse Fault System [DE-BY_1363], forms the reverse fault ramp for the movement of the crystalline rocks over the Permo-Mesozoic foreland, shaping the Bodenwöhr Trough.
Pfahl Shear Zone
Pfahl Scherzone
Das prägende Strukturelement des ostbayerischen Grundgebirges ist die Scherzone des Bayerischen Pfahls, eine im Perm angelegtes großräumiges Scherzonensystem, welches später mehrfach reaktiviert wurde. Typische Gesteine sind durch plastische (duktile) Deformation gebildete Mylonite („Pfahlschiefer“) und durch bruchhafte (spröde) Deformation entstandene Kataklasite. Morphologisch treten die verwitterungsresistenten, durch hydrothermale Aktivität und bruchhafte Deformation entstandenen polyphasen Quarzgangbreccien des Bayerischen Pfahls („Pfahlquarz“) am deutlichsten in Erscheinung und bilden häufig langgestreckte Härtlinge. Die ausgedehnten, insgesamt NW-SE verlaufenden Mylonit-Zonen des Pfahls werden bereichsweise von (sub-)parallelen Nebenstörungen und Quarzgängen [DE-BY_1361] begleitet und vereinzelt von den jüngeren Bayerwald Meridional Störungen [DE-BY_1350] versetzt.
The Pfahl Shear Zone, one of the most striking tectonic structures of the east-Bavarian Varican Basement rock suites, is a Permian large-scale shear zone system, reactivated multiply in later times. Generic rock types are mylonites (“Pfahl schist”) formed by ductile deformation and cataclastic rocks formed by brittle deformation. Evolving from hydrothermal activity and subsequent brittle tectonics, almost vertical polyphase quartz vein breccia (“Pfahl quartz”), due to their weathering resistance nowadays appearing as elongate monadnocks, are the most prominent physiographical feature. The extensive, overall NW-SE trending mylonite zones are, in certain areas, accompanied by (sub-)parallel subsidiary faults and quartz veins [DE-BY_1361] and sporadically displaced by the younger Bayerwald Meridional Faults [DE-BY_1350].
Pfahl Shear Zone Subsidiary Faults
Pfahl Scherzone Nebenstörungen
Pfahl Begleitstörungen
Neben den großräumigen Strukturelementen wie der Rundinger Zone [DE-BY_1348], die als Nebenast des Pfahl Scherzone [DE-BY_1362] gedeutet wird, und dem Aicha-Halser Nebenpfahl [DE-BY_762], die dem Donaustörungssystem [DE-BY_697] zugrechnet wird, wird die Pfahl Scherzone von kleinräumigen, (sub-)parallel und in räumlicher Nähe NW-SE streichenden Störungen und Quarzgängen begleitet , was eine generische und kinematische Verwandtschaft nahelegt. Die die Mylonitgrenzen spitzwinklig schneidenden Elemente werden als Fiederspalten-System interpretiert (Hofmann 1962).
Apart from the large-scale structural elements like Runding Zone [DE-BY_1348], construed as a branch of Pfahl Shear Zone [DE-BY_1362], and Aicha-Halser Nebenpfahl [DE-BY_762], assigned to Danube Fault System [DE-BY_697], Pfahl Shear Zone is accompanied by (sub-)parallel and close-by trending small-scale faults, implying a generic and kinematic relationship. Elements acute-angled to the boundaries of the mylonites are interpreted as tension gashes (Hofmann 1962).
Altendorf-Friedersried Fault
Altendorf-Friedersried Störung
NW-SE verlaufende, saigere bis sub-vertikale Störung, die spitzwinklig vom Nordwest-Ast der Pfahl Scherzone [DE-BY_1362] ausschert.
NW-SE trending, vertical to subvertical fault, acute-angled veering off the northwestern limb of Pfahl Shear Zone [DE-BY_1362].
Abteiland Diagonal Faults
Abteiland Diagonal Störungen
Kleinräumige, saiger bis steilstehende Störungen im südöstlichen Bayerischen Wald (Abteiland), die spitzwinklig vom WNW-ESE Haupttrend der Pfahl Scherzone [DE-BY_1362] abweichen und südlich des Pfahls ± NW-SE, nördlich des Pfahls ± WSW-ENE streichen. Diese Strukturen werden als "Pferdeschwanz"-Auffiederungen (horsetail splays) (Eberts et al. 2021) interpretiert oder können synthetische Wedel-förmige Auffiederungen der Hauptgleitfläche darstellen.
Array of small-scale vertical to subvertical faults in the southeastern Bavarian Forest (Abteiland), acute-angled veering off the principal WNW-ESE trend of the Pfahl Shear Zone [DE-BY_1362], and striking ± NW-SE south of the Pfahl, ± WSW-ENE north of the Pfahl. These structures are interpreted as horsetail splays (Eberts et al. 2021) or may be frond-like synthetic splays of the main fault zone plane.
Pfahl Reverse Fault System
Pfahl Aufschiebungssystem
Pfahlstörungszone
Von Pösing westlich Cham nach NW hin, wirkte der Bayerische Pfahl als Aufschiebungsfront des variszischen Grundgebirges der Böhmischen Masse auf das permo-mesozoische Vorland und bildet dabei den nordöstlichen Steilrand der Bodenwöhrer Senke. Westlich von Neukirchen-Balbini weicht der Verlauf des Pfahl Aufschiebungssystems leicht von der Pfahl Scherzone ab und bildet mit der unmittelbar südwestlich subparallel ziehenden Jura-Aufschiebung (Meyer & Mielke 1993) [DE-BY_1365] die Pfahl Störungszone (Meyer 2000), eine komplexe Aufschiebungszone entlang der steilen NE-Flanke der Bödenwöhrer Senke, die von einer intensiven jüngeren Quertektonik geprägt ist (wie die Bayerwald Meridional Störungen [DE-BE_1350] wahrscheinlich bei einer späteren Reaktivierung vergrößerte variszische R‘- und P‘-Riedelbrüche), hinter der die ältere Pfahltektonik zurücktritt (Meyer & Mielke 1993). Unter diesen Querstörungen ragt die Fensterbach Störung [DE-BY_970] heraus, die N von Freihöls die Pfahl Störungszone abschneidet und die Grenzlinie der Böhmischen Masse nach NNW ablenkt, wobei sich der Pfahl im permo-mesozoischen Vorland als „einzelne“ Aufschiebung nach WNW bis Amberg fortsetzt (Amberger Aufschiebung).
Roughly northwestwards from Pösing west of Cham the Bavarian Pfahl forms the reverse fault ramp for the movement of the Bohemian Massif Variscan Basement over the Permo-Mesozoic foreland, representing the northeastern scarp of the Bodenwöhr Trough. Forking off from the Pfahl Shear Zone west of Neukirchen-Balbini, and running close to and subparallel with the Jura Reverse Fault [DE-BY_1365], these two faults define the limits of Pfahl Fault Zone (Meyer 2000), a complex reverse fault system characterized by intense lateral tectonics (likewise Bayerwald Meridional Faults [DE-BY_1350] probably R’- and P’-Riedel shears of Variscan deformation, enlarged during later reactivation) outreaching the Variscan shearing and Alpine reverse faulting (Meyer & Mielke 1993). The most conspicuous of these lateral faults, Fensterbach Fault [DE-BY_970], deflects the western boundary line of the Bohemian Massif to the NNW and truncates the Pfahl Fault Zone in between the Pfahl and the Jura Reverse Faults, with the Pfahl continuing as a “single” reverse fault in the Permo-Mesozoic foreland further WNW-wards to Amberg (Amberger Aufschiebung).
Permo-Mesozoikum / Kristallin Randstörung
Erzhäuser-Blechhammer Fault
Erzhäuser-Blechhammer Störung
N-S verlaufende Querstörung des Pfahl Aufschiebungssystems [DE-BY_1366].
N-S trending lateral fault of Pfahl Reverse Fault System [DE-BY_1366].
Lateral Faults of Pfahl Reverse Fault System
Querstörungen des Pfahl Aufschiebungssystems
Post Pfahl Querstörungen die die Pfahl-Aufschiebung [DE-BY_1364] und Jura-Aufschiebung [DE-BY_1365] versetzen. Das Pfahl Aufschiebungssystems [DE-BY_1363] ist von einer intensiven jüngeren Quertektonik geprägt, hinter der die ältere Pfahltektonik (Meyer & Mielke 1993), als auch die alpidische Aufschiebungstektonik zurücktritt - wie die Bayerwald Meridional Störungen [DE-BE_1350] wahrscheinlich bei der späteren Reaktivierung vergrößerte variszische R‘- und P‘-Riedelbrüche.
Post Pfahl lateral faults offsetting the Pfahl Reverse Fault [DE-BY_1364] and Jura Reverse Fault [DE-BY_1365] within the Pfahl Reverse Fault System [DE-BY_1363] as the result of an intense tectonic outperforming the Variscan shearing (Meyer & Mielke 1993) and Alpine reverse faulting, thus of Miocene age or younger. Likewise Bayerwald Meridional Faults [DE-BY_1350] probably R’- and P’-Riedel shears of the Variscan deformation, enlarged during later reactivation.
Jura Reverse Fault
Jura-Aufschiebung
NW-SE verlaufene, steil nach NE einfallende Aufschiebung subparallel zur Pfahl Aufschiebung [DE-BY_1364] zwischen der Fensterbach Störung [DE-BY_970] und dem Cham Störungssystem [DE-BY_1408]. Bildet den SW Rand der Pfahl Störungszone (Meyer 2000) als nordöstlichem Steilrand der Bodenwöhrer Senke. Von zahlreichen Querstörungen [DE-BY_1366] des Miozäns oder jünger versetzt (Meyer & Mielke 1993).
NW-SE trending steeply NE dipping reverse fault running subparallel to Pfahl Reverse Fault [DE-BY_1364] between Fensterbach Fault [DE-BY_970] and Cham Fault System [DE-BY_1408] forming Pfahl Fault Zone (Meyer 2000) as the the northeastern scarp of the Bodenwöhr Trough. Offset by numerous lateral faults [DE-BY_1366] of Miocene age or younger (Meyer & Mielke 1993.
Pfahl Reverse Fault
Pfahl-Aufschiebung
Amberger Aufschiebung
Von Amberg bis Pösing W Cham, NW-SE verlaufende, steil nach NE einfallende Aufschiebung, entstanden durch variszische Scherung und alpidische Aufschiebung und durch zahlreiche jüngere Querstörungen [DE-BY_1366] segmentiert (Meyer & Mielke 1993). Zwischen ihrer Kreuzung mit der Fensterbach Störung [DE-BY_970] im NW und dem Cham Störungssystem [DE-BY_1408] im SE verläuft die Störung subparallel zur Jura Abschiebung [DE-BY_1365], und bildet dabei die NE Grenze der Pfahl Störungszone (Meyer 2000) als nordöstlichem Steilrand der Bodenwöhrer Senke.
Running from Amberg to Pösing west of Cham, NW-SE trending steeply NE dipping reverse fault featuring a Variscan shearing and Alpine reverse faulting and segmented by a later intense lateral tectonic [DE-BY_1366] (Meyer & Mielke 1993). Between its intersection with Fensterbach Fault [DE-BY_970] and Cham Fault System [DE-BY_1408] running subparallel to Jura Reverse Fault [DE-BY_1365], forming Pfahl Fault Zone (Meyer 2000) as the the northeastern scarp of the Bodenwöhr Trough.
Hildenbach Fault
Hildenbach Störung
NW-SE streichende Störung südlich der Schnaittenbacher Störung [DE-BY_1468].
NW-SE striking fault south of Schnaittenbach Fault [DE-BY_1468].
Schmidgaden Rotliegend Graben boundaries
Schmidgaden Rotliegend-Graben Randstörungen
WNW-ESE verlaufende Störungen, teilweise N-S versetzt, in der Verlängerung der Pfahl Scherzone [DE-BY_1362] und subparallel zum Pfahl Aufschiebungssystem [DE-BY_1363], im Westen von der Fensterbach Störung [DE-BY_970] abgeschnitten.
WNW-ESE trending faults with N-S offsets, on strike of Pfahl Shear Zone [DE-BY_1362] and subparallel to Pfahl Reverse Fault System [DE-BY_1363]; truncated by Fensterbach Fault [DE-BY_970] in the west.
Wölsendorf Fault
Wölsendorf Störung
WNW-ESE streichende Störung in der Verlängerung der Pfahl Scherzone [DE-BY_1362] und subparallel zum Pfahl Aufschiebungssystem [DE-BY_1363].
WNW-ESE striking fault on strike of Pfahl Shear Zone [DE-BY_1362] and subparallel to Pfahl Reverse Fault System [DE-BY_1363].
Pamsendorf Fault Set
Pamsendorf Störungsschar
Schar W-E verlaufender, saigerer bis subvertikaler Störungen.
Array of W-E trending vertical to subvertical faults.
Upper Palatine Forest SW-NE faults
SW-NE Störungen des Oberpfälzer Waldes
SW-NE verlaufende, saigere bis subvertikale Störungen südlich der Luhe Störung [DE-BY_965], zwischen der Cham Störung [DE-BY_1408] und dem Naabgebirge, dem westlichen Sporn des Oberpfälzer Waldes.
SW-NE trending vertical to subvertical faults south of Luhe Fault [DE-BY_965], between Cham Fault [DE-BY_1408] and Naabgebirge, the western spur of Upper Palatine Forest.
Schnaittenbach Fault
Schnaittenbacher Störung
Demenrichter Sörung
NNW-SSE verlaufende, ca. 60° nach WSW einfallende Aufschiebung des Grundgebirges auf die triassischen Einheiten im Osten.
NNW-SSE trending, approx. 60° WSW dipping reverse fault, thrusting the Variscan basement onto the Triassic deposits in the east.
Weidelbach Fault
Weidelbach Störung
In nördlicher Verlängerung der Schnaittenbacher Störung [DE-BY_1467] NNW-SSE verlaufende Störung mit geringer Sprunghöhe in triassischen Schichten.
NNW-SSE trending intra-Triassic minor throw fault northward on-strike of Schnaittenbach Fault [DE-BY_1467].
Neuersdorf Fault
Neuersdorfer Störung
In nördlicher Verlängerung der Kemnather Störung [DE-BY_1465] gewellt N-S verlaufende Störung mit geringer Sprunghöhe in triassischen Schichten.
Undulate N-S trending intra-Triassic minor throw fault northward on-strike of Kemnath Fault [DE-BY_1465].
Saxothuringian Zone tectonic boundaries
Tektonische Grenzflächen der Saxothuringischen Zone
Das Saxoturingium, der Teil der Böhmischen Masse nördlich der Erbendorfer Line [DE-BY_1447], der von „minimal“-metamorphen (anchimetamorphen) Gesteinen aufgebaut wird, ist durch NW-SE (steil herzynisch) bis WNW-ESE (flach herzynisch) verlaufende Störungen und Störungsscharen gekennzeichnet. Grob SW-NE streichende Störungen folgen i.d.R. den Trends von Großstrukturen wie der Erbendorfer Line [DE-BY_1447] oder der Längsseite der Münchberger Masse Basis-Überschiebung [DE-BY_1504], oder, besonders im Frankenwald, folgen den Faltenachsen der Einengungstektonik des Unterkarbons (Mississippium).
The Saxothuringian Zone, the Bohemian Massif realm north of Erbendorf Line [DE-BY_1447] featuring very low grad metamorphic (anchimetamorphic) rocks, is characterized by NW-SE (high-angle Hercynian) to WNW-ESE (flat-angle Hercynian) trending faults and fault sets. The faults roughly trending SW-NE generally are paralleling major tectonic structures, such as Erbendorf Line [DE-BY_1447] or the longside of Münchberg Klippe basal thrust [DE-BY_1504], or, specifically in Franconian Forest, follow the fold axes of compressional tectonics during Early Carboniferous (Mississippian).
Trebesbach Fault
Trebesbach Störung
WNW-ESE verlaufende, südwestlichster Querbruch der Teuschnitzer Mulde, subparallel zum Frankenwald-Randbruch [DE-BY_1431].
WNW-ESE trending, southwestern-most Teuschnitz Syncline lateral fault, running subparallel Franconian Forest Scarp [DE-BY_1431].
Teuschnitz Syncline lateral faults
Querbrüche der Teuschnitzer Mulde
NW-SE verlaufende Schrägabschiebungen die die Faltenachsen bis zu wenigen hundert Metern versetzen. Im Endstadium der Faltung als linkssinnige Blattverschiebungen angelegt, wurden die Brüche im jüngeren Tertiär als Abschiebungen reaktiviert.
NW-SE trending oblique-slip faults offsetting the fold axes up to few hundreds of meters. Formed as sinistral strike-slip lateral disruptions in the final stage of folding and reactivated as normal faults during younger Tertiary.
Teuschnitz Syncline longitudinal faults
Faltungsbrüche der Teuschnitzer Mulde
Parallel zu den Faltenachsen SW-NE verlaufende, steil nach NW einfallende Aufschiebungen, als Ergebnis der spät-synsedimentär einsetzenden Einengungstektonik des Unterkarbons (Mississippium).
SW-NE trending steeply NW dipping reverse faults parallel to the fold axes, due to late depositional to immediately post-depositional compression tectonics during Early Carboniferous (Mississippian).
Arzberg Fault
Arzberger Störung
Arzberger Linie
Insgesamt SW-NE verlaufende, steil nach SW einfallende Abschiebung; Nordrand des Waldsassener Schiefergebirges, von den Arzberg Querstörungen [DE-BY_1524] mehrfach versetzt.
Overall SW-NE trending, steeply SW dipping normal fault, northern boundary of Waldsassen Slate Mountains (Waldsassener Schiefergebirge), multiply offset by Arzberg lateral faults [DE-BY_1524].
Birkstauden-Hardeck Fault
Birkstauden-Hardeck Störung
WSW-ENE verlaufende, steil nach SSE einfallende Störung die von der Erbendorfer Linie [DE-BY_1447] abzweigt; wird von herzynischen Störungen des Stiftslands [DE-BY_1455] und von der Poxdorf Störung [DE-BY_1493] versetzt.
WSW-ENE trending, steeply SSE dipping fault branching of Erbendorf Line [DE-BY_1447], offset by Stiftsland Hercynian faults [DE-BY_1455] and Poxdorf Fault [DE-BY_1493].
Holzmühle-Mohelenská pláň Fault
Holzmühle-Mohelenská pláň Störung
SW-NE verlaufende, steil nach SE einfallende listrische Aufschiebung im südlichen Waldsassener Schiefergebirge subparallel zur Pilmersreuth-Mähring Störung [DE-BY_1490] bzw. Erbendorfer Linie [DE-BY_1447]; mehrfach von herzynischen Störungen des Stiftslands [DE-BY_1455] versetzt.
SW-NE trending, steeply SE dipping listric reverse fault crossing the southern Waldsassen Slate Mountains (Waldsassener Schiefergebirge) subparallel to Pilmersreuth-Mähring Fault [DE-BY_1490] resp. Erbendorf Line [DE-BY_1447]; multiply offset by Stiftsland Hercynian faults [DE-BY_1455].
Blaue Leite-Moos Fault
Blaue Leite-Moos Störung
Gewellt SW-NE verlaufende, steil nach NW einfallende Abschiebung zwischen Kemlaser Störung [DE-BY_1437] und Gupfen Störung [DE-BY_1520], SE-wärts versetzte Fortsetzung der südlichen Issigauer Störung [DE-BY_1438], als Begrenzung eines Karbon "Horstes" im NW gegen Devon-Ablagerungen im SE.
Undulate SW-NE trending steeply NW dipping normal fault in between Kemlas Fault [DE-BY_1437] and Gupfen Fault [DE-BY_1520], SE-ward displaced eastern continuation of southern Issigau Fault [DE-BY_1438] offsetting a Carboniferous "Horst" in NW from Devonian deposits in SE.
Rudolphstein Fault
Rudolphstein Störung
NW-SE streichende linkssinnige Blattverschiebung; versetzt die Issigauer Störungen [DE-BY_1438] ca. 800 m nach NW.
NW-SE striking sinistral strike-slip fault offsetting Issigau Faults [DE-BY_1438] approx. 800 m to NW.
Gupfen Fault
Gupfen Störung
NW-SE streichende rechtssinnige Blattverschiebung; versetzt die Issigauer Störungen [DE-BY_1438] ca. 1 km nach SE.
NW-SE striking dextral strike-slip fault offsetting Issigau Faults [DE-BY_1438] about 1 km to SE.
Neugattendorf-Regnitzlosau Fault
Neugattendorf-Regnitzlosau Störung
NW-SE verlaufende Störung östlich von Hof.
NW-SE trending fault east of Hof.
Stiftsland Hercynian faults
Herzynische Störungen des Stiftslands
WNW-ESE (flach herzynisch) streichende, saigere bis subvertikale Blatt- oder Schrägverschiebungen; versetzen am Südrand des Saxothurigium die Pilmersreuth-Mähring Störung [DE-BY_1490].
WNW-ESE striking, vertical to subvertical strike-slip or oblique-slip faults offsetting Pilmersreuth-Mähring Faul [DE-BY_1490] at the southern boundary of Saxothuringian Zone.
Poxdorf Fault
Poxdorf Störung
WNW-ESE bis NW-SE streichende, saigere bis subvertikale linkssinnige Blatt- oder Schrägverschiebung; versetzt die Birkstauden-Hardeck Störung [DE-BY_1498].
WNW-ESE to NW-SE striking, vertical to subvertical sinistral strike-slip or oblique-slip fault offsetting Birkstauden-Hardeck Fault [DE-BY_1498].
Muglberg-Mähring Fault
Muglberg-Mähring Störung
WNW-ESE (flach herzynisch) streichende, saigere bis subvertikale linkssinnige Blatt- oder Schrägverschiebung; versetzt die Pilmersreuth-Mähring Störung [DE-BY_1490] geringfügig.
WNW-ESE striking, vertical to subvertical sinistral strike-slip or oblique-slip fault slightly displacing Pilmersreuth-Mähring Fault [DE-BY_1490]
Issigau Faults
Issigauer Störungen
SW-NE verlaufende, steil nach NW einfallende Abschiebungen als Begrenzung eines Karbon "Horstes" zwischen devonischen Ablagerungen. Von der Kemlaser Störung [DE-BY_1437] ca. 800 m nach NW und, weiter im NE, von der Gupfen Störung [DE-BY_1520] ca. 1 km nach SE versetzt.
SW-NE trending, steeply NW dipping normal faults confining a Carboniferous "Horst" within Devonian deposits. Offset approx. 800 m to NW by Kemlas Fault [DE-BY_1437] and, further to NE, about 1 km to SE by Gupfen Fault [DE-BY_1520].
Höllbach-Neuhausen Fault
Höllbach-Neuhausen Störung
NNW-SSE verlaufende, saigere bis subvertikale rechtsinnige Schrägabschiebung SE von Rehau.
NNW-SSE trending, vertical to subvertical dextral oblique-slip normal fault SE of Rehau.
Kemlas Fault
Kemlaser Störung
Gebogen NW-SE bis WNW-ESE verlaufende, steil nach SW einfallende linkssinnige Schrägabschiebung, in Abschnitten als Flußspat Gänge. Versetzt die Issigauer Störungen [DE-BY_1438] ca. 800 m nach NW; Teil der Südwest-Grenze der Frankenwälder Querzone.
Arcuate NW-SE to WNW-ESE trending, steeply SW dipping sinistral oblique-slip normal fault, in segments manifested as flourite veins, offsetting Issigau Faults [DE-BY_1438] approx. 800 m to NW. Part of southwestern boundary of Frankenwälder Querzone (Franconian Forest Lateral Zone).
Buchbach Fault
Buchbach Störung
NNW-SSE streichende linkssinnige Schrägabschiebung.
NNW-SSE striking sinistral oblique-slip normal fault.
Keilstein Fault
Keilstein Störung
NW-SE verlaufende, steil nach SW einfallende linkssinnige Schrägabschiebung; Teil der Südwest-Grenze der Frankenwälder Querzone.
NW-SE trending steeply SW dipping sinistral oblique-slip normal fault, part of southwestern boundary of Frankenwälder Querzone (Franconian Forest Lateral Zone).
Tettau Fault
Tettau Störung
Schar NW-SE streichender linkssinniger Schrägabschiebungen.
Set of NW-SE striking sinistral oblique-slip normal faults.
Epplas Fault
Epplaser Störung
NW-SE verlaufende, polyphas rechtssinnige Schrägverschiebung mit einem Vertikalversatz von etwa 1 km, die die Überschiebungsflächen sowohl der Bayerische Fazies [DE-BY_1525] als auch der Münchberger Masse [DE-BY_1504] versetzt bzw. abschneidet. Mäßig steil bis steil nach SW einfallende, oft mylonitisierte Störung prä-variszischer Entstehung und variszisch reaktiviert, zunächst als Schrägaufschiebung, später Abschiebung.
NW-SE trending major structure offsetting / truncating the Bavarian Facies basal thrust [DE-BY_1525] as well as the Münchberg Klippe basal thrust [DE-BY_1504]. Intermediate to steeply SW dipping polyphase dextral oblique-slip fault, partly mylonite, featuring a vertical throw of about 1 km. Pre-Variscan origin, Variscan reactivation as an oblique-slip reverse fault, later normal fault.
Ludwigsstadt-Lauenhain Fault
Ludwigsstadt-Lauenhain Störung
Südwestliche Flanke des Gräfenwalder Horstes, einer der Hauptstrukturen der Frankenwälder Querzone.
NW-SW trending southwestern flank of Gräfenwald Horst, a principal structure of Franconian Forest transverse zone (Frankenwälder Querzone).
Ludwigsstadt Fault
Ludwigsstadt Störung
W-E streichende Störung bei Ludwigstadt, versetzt den Gräfenwalder Horst nach Westen.
W-E striking fault at Ludwigstadt, displacing Gräfenwald Horst to the west.
Ebersdorf-Teuschnitz Fault
Ebersdorf-Teuschnitz Störung
NW-SE verlaufende Störung, bildet in ihrem nördlichen Abschnitt die südwestliche Flanke des Gräfenwalder Horstes, einer der Hauptstrukturen der Frankenwälder Querzone.
NW-SE trending fault, in its northern segment representing the southwestern boundary of Gräfenwald Horst, a principal structure of Franconian Forest transverse zone (Frankenwälder Querzone).
Wiedersberg Fault
Wiedersberger Störung
Wiedersberger Gang
NW-SE verlaufende, mäßig steil nach SW einfallende rechtssinnige Schrägabschiebung.
NW-SE trending, intermediately SW dipping, dextral oblique slip normal fault.
Joditz Fault
Joditzer Störung
Von Ludwigshöhe durch die Vogtland Mulde bis Unterkotzau ziehende, NW-SE verlaufende, mäßig steil nach SW einfallende rechtssinnige Schrägabschiebung.
Running from Ludwigshöhe to Unterkotzau across Vogtland syncline, NW-SE trending, intermediately SW dipping, dextral oblique-slip normal fault.
Bärenholz Fault
Bärenholz Störung
Nordhalben-Lotharheil Fault
Nordhalben-Lotharheil Störung
NNW-SSE verlaufende, subvertikale bis steil nach WSW einfallende Störung.
NNW-SSE trending, subvertical to steeply ENE dipping fault.
Dürrenwaid Fault
Dürrenwaid Störung
NNW-SSE trending, subvertical to steeply WSW dipping fault.
Münchberg Klippe faults
Münchberger Überschiebungsinsel Störungen
Zwischen Frankenwald und Fichtelgebirge liegt eine fremdartige Gesteinsscholle - die Münchberger Masse - schüsselförmig eingesenkt im saxothuringischen Grundgebirge aus paläozoischen Gesteinen der Bayerischen Fazies über Thüringer Fazies. Die Münchberger Gneissmasse wird als Überschiebungsinsel (Klippe) eines inversen (höchster Metamorphosegrad am Top) Deckenstapels interpretiert, dessen Einheiten im Devon bis Unterkarbon übereinandergeschoben wurden. Die Basis der Müchberger Klippe und der unterlagernden und umgebenden Bayerischen Fazies werden von flachen Überschiebungen gebildet, die spät- bis postvariszisch zerlegt wurden und von einer steilstehenden, verschuppten im Südosten-Grenze zum Fichtelgebirge.
In between the Fichtel Mountains to the southeast and the Franconian Forest to the northwest, an exotic block - the Münchberg Klippe - bowl-like rests upon the Saxothuringian basement made up of Bavarian Facies Paleozoic deposits thrusted over Thuringian Facies Paleozoic rocks. Münchberg Klippe is considered a thrust-outlier featuring an inverse stack of nappes with the highest-grade metamorphic rocks on top, piled up by thrusting during Devonian and Early Carboniferous (Mississippian). Münchberg Klippe basal thrust, as well as the thrust plain of its fringe and footwall - Bavarian Facies - form flat overthrusts disaggregated by late and post-Varican faulting and a steep, imbricate southeastern boundary towards Fichtel Mountains rock association.
Münchberg Klippe basal thrust
Münchberger Masse Basis-Überschiebung
SW-NE gestreckt schüsselförmige, flach bis mäßig steil einfallende Überschiebungsfläche der Basis der Münchberger Masse über die Bayerische Fazies. Von den Münchberger Masse Quer-Störungen [DE-BY_1434] zerlegt und entlang der Fränkischen Linie [DE-BY_1398] abgeschnitten bzw. vertikal versetzt. Die steil einfallende und verschuppte Südost-Grenze ist das Ergebnis NW-SE einengender Bruchtektonik und Scherung.
SW-NE elongated bowl-shaped gently dipping thrust plane of Münchberg Klippe base over the Bavarian Facies realm; disaggregated by Münchberg Klippe lateral faults [DE-BY_1434] and offset resp. downwarped along Franconian Line [DE-BY_1398] in the southwest. The sheer imbricate eastern boundary results from NW-SE compressional brittle tectonics and shearing.
Bavarian Facies basal thrust
Bayerische Fazies Basis-Überschiebung
Basis der Bayerischen Fazies als unterste und äußere Überschiebung der Münchberger Klippe s. l.. Im Norden und Nordosten von Frankenwald Störungen zerlegt und verschoben und entlang der Fränkischen Linie [DE-BY_1398] abgeschnitten bzw. vertikal versetzt. Die steil einfallende und verschuppte Südost-Grenze ist das Ergebnis NW-SE einengender Bruchtektonik und Scherung.
Lowest and outermost thrust of Münchberg Klippe s. l. stack of nappes, gently dipping basal thrust of the Bavarian Facies realm. In the northern and northwestern part disaggregated and offset by Franconian Forest faults and truncated resp. downwarped along Franconian Line [DE-BY_1398] in the southwest. Its sheer imbricate southeastern boundary results from NW-SE compressional brittle tectonics and shearing.
Elbersreuth-Schwarzenstein-Schwarzenbach Fault
Elbersreuth-Schwarzenstein-Schwarzenbach Störung
Insgesamt SSW-NNE verlaufender interne Überschiebung in der Bayerischen Fazies.
Overall SSW-NNE trending internal thrust within the Bavarian Facies.
Geuser-Wallenfels Fault
Geuser-Wallenfels Störung
Gewellt SSW-NNE verlaufende Störung, im nördlichen Abschnitt nordöstliche Begrenzung des Wallenfels Sporns der Bayerischen Fazies.
Undulate SSW-NNE trending fault, in ist northern part northeastern boundary of Bavarian Facies Wallenfels spur.
Wurbach-Wallenfels Fault
Wurbach-Wallenfels Störung
Gewellt SW-NE verlaufende Störung, abschnittsweise nordwestliche Begrenzung des Wallenfels Sporns der Bayerischen Fazies.
Undulate SW-NE trending fault, in segments northwestern boundary of Bavarian Facies Wallenfels spur.
Münchberg Klippe lateral faults
Münchberger Masse Quer-Störungen
Grob NW-SE verlaufende Störungen der Münchberger Masse, die die Münchberger Masse Basis-Überschiebung [DE-BY_1504] Ränder sowie die internen Überschiebungen des Deckenstapels versetzen.
Roughly NW-SE trending faults of Münchberg Klippe, offsetting Münchberg Klippe basal thrust [DE-BY_1504] margins and the (internal) thrusts of the stack of nappes.
Münchberg Klippe longitudinal faults
Münchberger Masse Längs-Störungen
SW-NE verlaufende Störungen der Münchberger Masse.
SW-NE trending faults of Münchberg Klippe.
Heinersgrün Step Fault
Heinersgrün Bruchstaffel
NNW-SSE verlaufende Bruchstaffel subvertikal bis steil nach ENE einfallender linkssinniger Schrägabschiebungen.
NNW-SSE trending, step fault of subvertical to steeply ENE dipping sinistral oblique-slip normal faults.
Bad Steben Fault Zone
Bad Stebener Störungszone
Von Carlsgrün nach Bobengrün NNW-SSE verlaufende, den Bergaer Sattel schneidende Grabenstruktur an deren Flanken Säuerlinge und Mineralgänge zu Tage treten.
Running from Carlsgrün to Bobengrün crossing Berga anticline, NNW-SSE trending graben structure featuring acidulous springs and mineral veins at its flanks.
Mordlau-Bobengrün faults
Mordlau-Bobengrün Störungen
Östliche Flanke des Bad Stebener Grabens; NNW-SSE verlaufende, steil nach WSW einfallende Abschiebungen mit einer Sprunghöhe von bis zu 300 m, teilweise als Siderit-Gänge (Mordlauer Gangzug).
Eastern scarp of Bad Steben Graben. NNW-SSE trending, steeply WSW dipping normal faults featuring a throw of up to more than 300 m, partly manifested as siderite veins (Mordlau train of veins).
Carlsgrün-Horwagen faults
Carlsgrün-Horwagen Störungen
Westliche Flanke des Bad Stebener Grabens; NNW-SSE verlaufende, steil bis subvertikal nach ENE einfallende Abschiebungen mit einer Sprunghöhe bis zu 250 m, Aufstiegsbruch der Bad Stebener Säuerlinge.
Western scarp of Bad Steben Graben. NNW-SSE trending, steeply to subvertical ENE dipping normal faults featuring a cumulative throw of up to 250 m; feeder conduits of Bad Steben acidulous springs.
Fichtel Mountains faults
Fichtelgebirge Störungen
Das Fichtelgebirge zwischen der Erbendorfer Linie [DE-BY_ 1447] bzw. dem Waldsassener Schiefergebirge im Süden und der Münchberger Masse [vgl. DE-BY_1503] im Norden, wird von variszischen gering metamorphen und - vorherrschend - Granit Intrusionen aufgebaut. Drei Hauptrichtungen bestimmen das Störungsmuster der spätvariszisch angelegten und mehrfach (v.a. durch Krustenbewegungen der alpidischen Gebirgsbildung), zuletzt im Tertiär reaktivierten Störungen: WNW-ESE, NW-SE und SW-NE.
The Fichtel Mountains, in between the Erbendorf Line [DE-BY_ 1447] resp. Waldsassen Slate Mountains (Waldsassener Schiefergebirge) to the south and Münchberg Klippe [cf. DE-BY_1503] to the north, is made up of Varican low-grade metamorphic, folded sedimentary rocks and predominant granite intrusions. Three principal trends prevail the pattern of the late-Variscan faults, multiply reactivated mainly due to Alpine Orogeny crustal movements, lastly in Tertiary: WNW-ESE, NW-SE, and SW-NE.
Fichtel Mountains lateral faults
Fichtelgebirge Quer-Störungen
Insbesondere im Nahbereich der Fränkischen Linie [DE-BY_1398], hier: Fichtelgebirgs-Randbruch [DE-BY_1432], verbreitete, NW-SE gerichtete, mit Annäherung an den Fichtelgebirgs-Randbruch auf NNW-SSE drehende Störungen.
Particularly widespread close to the Franconian Line [DE-BY_1398], here: the Fichtel Mountains Scarp [DE-BY_1432], NW-SE trending faults, veering to NNW-SSE when converging Fichtel Mountains Scarp.
Fichtel Mountains Hercynian faults
Herzynische Störungen im Fichtelgebirge
Flach herzynisch (WNW-ESE) streichende Störungen vorwiegend in den Metasedimenten am Nordost-Rand des Fichtelgebirges.
WNW-ESE (flat-angle Hercynian) striking faults predominantly in the meta-sediments of Fichtel Mountains northeastern margin.
Fichtel Mountains longitudinal faults
Fichtelgebirge Längs-Störungen
SW-NE verlaufende, saigere bis subvertikale Störungen parallel zu den Faltenachsen, vorwiegend in den Metasedimenten am Nordost-Rand des Fichtelgebirges.
SW-NE trending, vertical to subvertical faults parallel to the fold axes, predominantly in the low-grade meta-sediments of Fichtel Mountains northeastern margin.
Selbitztal Fault
Selbitztal Störung
Von Naila nach Selbitz ziehende, NW-SE bis WNW-ESE verlaufende Störung die den Garleswald Sporn der Bayerische Fazies im NE abschneidet und die Bayerische Fazies Basis-Überschiebung [DE-BY_1525] versetzt.
Running from Naila to Selbitz, NW-SE to WNW-ESE trending fault truncating Bavarian Facies Garleswald spur in the NE thus offsetting the Bavarian Facies basal thrust [DE-BY_1525].
Arzberg lateral faults
Arzberg Querstörungen
NW-SE bis N-S verlaufende Störungen ± senkrecht zur Arzberger Störung [DE-BY_1499], die von den Querstörungen versetzt wird.
Set of NW-SE to N-S trending faults ± perpendicular to and offsetting Arzberg Fault [DE-BY_1499].
Feilitzsch Fault
Feilitzsch Störung
NW-SE verlaufende rechtssinnige Schrägabschiebung.
NW-SE trending dextral oblique slip normal fault.
Bohemian Massif Western Margin tectonic boundaries
Durchquert auf mehr als 150 km bayerisches Gebiet, insgesamt NW-SE verlaufender Großschollenrand der die Böhmische Masse gegen das Süddeutsche Schichtstufenland begrenzt, meist in Form nach ± E einfallender Auf- und Überschiebungen. Mehrfach versetzt durch Quer-Störungssysteme und abschnittsweise durch jüngere Bildungen verdeckt. Wird im Süden vom Donaustörungssystem [DE-BY_697] abgeschnitten bzw. nach Osten und Südosten hin abgelenkt. Variszisch angelegt und danach mehrfach reaktiviert, erfolgte die Hauptphase der Heraushebung des Westrandes der Böhmischen Masse und Aufschiebung auf das permo-mesozoische Vorland während der Oberkreide und des Paläogens (Bayerisches Geologisches Landesamt 1996).
The Bohemian Massif Western Margin tectonic boundaries can be directly observed only in very few segments. In most cases, the faults’ trend is inferred from contour lines pattern of the Permo-mesozoic foreland and/or extrapolated from outcrop evidence, aligned with geophysical surveys interpretations or remote sensing data in few areas. As a rule, the top of the Varican basement serves as the reference horizon for the indication of the vertical displacement (throw). As the exposed Bohemian Massive has been subject to intense peneplanation during Tertiary, the figures given, thus, represent the present-day “residual” throw.
Die tektonischen Bauelemente des Westrands der Böhmischen Masse können nur in wenigen Abschnitten direkt kartiert werden. Der Verlauf der Störungen ist größtenteils aus Streichlinien-Mustern im permo-mesozoischen Vorland abgeleitet und/oder aus Aufschluss-Befunden extrapoliert, im Kontext mit Fernerkundungsdaten und geophysikalischen Untersuchungen in ausgesuchten Gebieten. Für die Ermittlung des vertikalen Versatzes (Sprunghöhe) wird in der Regel die Oberfläche des Grundgebirges herangezogen. Da die zu Tage tretende Böhmische Masse insbesondere im Tertiär einer intensiven Einrumpfung unterlag, sind die ermittelten Sprunghöhen aktuelle (Residual-) Werte.
Traversing Bavarian territory for more than 150 km, overall NW-SE trending borderline separating the Bohemian Massif to the east from the South German Scarpland to the west, primarily as a ± E dipping reverse or thrust fault (system). Multiply displaced by transverse fault systems and in sections obscured by younger deposits. In the south, truncated / deflected by the Danube Fault System [DE-BY_697] towards the east and southeast. Evolving during Variscan orogeny, afterward multiply reactivated, the main phase of the uplift of the western marginal zone of the Bohemian Massif, overthrusting the Permo-Mesozoic foreland, took place during Upper Cretaceous and Paleogene (Bayerisches Geologisches Landesamt 1996).
Tektonische Grenzflächen des Westrands der Böhmischen Masse
Bohemian Massif Western Margin System
Störungssysteme des Westrands der Böhmischen Masse
Schwarzenfeld Fault
Schwarzenfeld Störung
SSW-NNE streichende, unter dem Naabtal Tertiär verborgene Schrägabschiebung, die das Pfahl Aufschiebungssystem [DE-BY_1363] ca. 1 km sinistral versetzt. Die wahrscheinlich W-vergente Störung weist eine von S nach N zunehmende Sprunghöhe bis zu 40 m auf.
SSW-NNE striking oblique slip fault underneath the Tertiary deposits of Naab River Valley, displacing the Pfahl Reverse Fault System [DE-BY_1363], for about 1 km in a sinistral offset. The probably W dipping fault features, from S to N increasing, a throw of up to 40 m.
Krondorf Fault
Krondorf Störung
N-S streichender Ast der Schwarzenfeld Störung [DE-BY_1373] mit einem Verwurf von bis zu 20 m.
N-S striking branch of Schwarzenfeld Fault [DE-BY_1373] featuring a throw of up to 20 m.
Luhe Line
Luhe Linie
SW-NE bis W-E verlaufende Störungslinie, die die Westgrenze der Böhmischen Masse um über 25 km versetzt. Westlich der Freihung Störung [DE-BY_990] nur in kurzen Abschnitten nachweisbar.
SW-NE to W-E trending fault line offsetting the western margin of the Bohemian Massif for more than 25 km. West of Freihung Fault [DE-BY_990] evidenced in short sections only.
Luhe Fault
Luhe Störung
Luhe Fault System
Luhe Störungssystem
Neudorfer Störung
Overall W-E trending, steeply S dipping polyphase reverse fault with a (final) rotational movement forming a scissors-fault (“tilted blocks crossover”, Steinlein 1953) with the pivot near Neudorf. In the west, featuring a throw of more than 400 m, the northern block forms the footwall, in the east, with a throw of up to more than 120 m, the hanging wall (Bauberger & Haunschild 1960). Kinematic history comprises reverse faulting during late Carboniferous, normal reactivation in early Cretaceous, and the late Cretaceous / early Tertiary rotational movement, i.e. inversion in the western part while normal reactivation in the eastern part (Peterek & Schröder 2017). East of Franconian Line [DE-BY_1398] resp. its southernmost section Gleitsbach-Windbühl Fault [DE-BY_1399] Luhe Fault forms the southern boundary of Erbendorf-Vohenstrauss Zone (ZEV), an outlier of Teplá-Barrandian Block.
Insgesamt W-E verlaufende, steil Süd-fallende polyphase Aufschiebung mit einer (abschließenden) Rotationsbewegung, d.h. Scherenstörung (Kippschollen-Kreuzung nach Steinlein 1953), mit einer Drehachse bei Neudorf. Im Westen ist bei einer Mindestsprunghöhe von mehr als 400 m die nördliche Scholle herausgehoben, im Osten, bei einer Sprunghöhe bis über 120 m, die Südscholle (Bauberger & Haunschild 1960). Die kinematische Geschichte umfasst eine aufschiebende Tektonik im späten Karbon, eine abschiebende Reaktivierung in der frühen Kreide und, in der späten Kreide / Jungtertiär, eine Rotationsbewegung mit aufschiebender Inversionstektonik im westlichen Teil bei abschiebender Reaktivierung im östlichen Teil (Peterek & Schröder 2017). Östlich der Fränkischen Linie [DE-BY_1398] bzw. ihres südlichsten Abschnitts, der Gleitsbach-Windbühl Störung [DE-BY_1399], definiert die Luhe Störung die Südgrenze der Zone von Erbendorf-Vohenstrauß (ZEV), einer Überschiebungsinsel des Teplá-Barrandiums.
Engelshof Subfault
Engelshof Nebenstörung
WSW-ENE bis W-E verlaufender Nord-Ast der Luhe Störung an der Kreuzung der Luhe Linie [DE-BY_1387] mit der Fränkischen Linie [DE-BY_1398].
WSW-ENE to W-E trending northern branch of Luhe Fault at the intersection of Luhe Line [DE-BY_1387] and Franconian Line [DE-BY_1398].
Kindlas Fault
Kindlas Störung
W-E verlaufende, steil nach N einfallende Aufschiebung als Verbindung der nach NW abdrehenden Luhe Störung [DE-BY_965] und der NW-SE verlaufenden Freihunger Störung [DE-BY_990].
W-E trending, steeply N dipping reverse fault connecting Luhe Fault [DE-BY_965] veering to the NW and NW-SE trending Freihung Fault [DE-BY_990].
Ehenbach Fault
Ehenbach Störung
WSW-ENE streichende Störung mit geringen Versatz als vermutete Verbindung zwischen der Krickelsdorf-Kainsricht Störung [DE-BY_1381] und Kindlas Störung [DE-BY_1384].
WSW-ENE striking fault featuring a minor throw, as the inferred link of Krickelsdorf-Kainsricht Fault [DE-BY_1381] and Kindlas Fault [DE-BY_1384].
Krickelsdorf-Kainsricht Fault
Krickelsdorf-Kainsrichter Störung
SW-NE streichende Störung mit geringem Versatz als westliches Ende der Luhe Linie.
SW-NE striking fault featuring a minor throw, as the inferred western termination of Luhe Line.
Fensterbach Fault
Fensterbach Störung
Fensterbach-Aufschiebung
Naabgebirgs-Randstörung
Von Gebenbach SW Hirschau bis Dürnsricht ziehende, großenteils dem von NNW-SSE auf NW-SE umbiegenden Fensterbachtal folgende, steil nach ± NE einfallende Aufschiebung mit einem Versatz von bis zu über 200 m. Südwestgrenze des Naabgebirges als westlicher Sporn der Böhmischen Masse. Schneidet sowohl die Jura-Aufschiebung [DE-BY_1365] des Pfahl Aufschiebungssystems [DE-BY_1363], als auch den Rotliegendgraben von Schmidgaden im Westen ab. Eine Verbindung zur Pittersberger Störung [DE-BY_1374] im Süden wird vermutet (Bauberger & Streit 1982), ist aber nicht nachgewiesen.
Running from Gebenbach SW Hirschau on to Dürnsricht, largely tracing the Fensterbach Valley veering from NNW-SSE to NW-SE, steeply NE dipping reverse fault with a throw of up to more than 200 m. Southwestern borderline of the Naabgebirge, the western spur of the Bohemian Massif. Truncating the Jura Reverse Fault [DE-BY_1365] of the Pfahl Reverse Fault System [DE-BY_1363], as well as the Schmidgaden Rotliegend Graben, in the west. A connection / soft link with Pittersberg Fault [DE-BY_1374] in the south is assumed (Bauberger & Streit 1982) but not evidenced.
Wenzelberg Fault
Wenzelberg Störung
SW-NE verlaufende Grenzlinie zwischen der Permotrias im Norden und dem variszischen Grundgebirge im Süden.
SW-NE trending fault marking the borderline between the Permo-Triassic to the north and the Variscan Basement to the south.
Scharhof Fault
Scharhof Störung
NNW-SSE verlaufende, ca. 60° nach WSW einfallende Aufschiebung mit einer Sprunghöhe von bis zu 35 m.
NNW-SSE trending, approx. 60° WSW dipping reverse fault featuring a throw of up to 35 m.
Brunnhof Fault
Brunnhof Störung
NW-SE bis N-S verlaufende Querstörung zur Krickelsdorf-Kainsricht Störung [DE-BY_1381]. Abschiebung mit einer Sprunghöhe bis zu 40 m.
NW-SE to N-S trending lateral fault of Krickelsdorf-Kainsricht Fault [DE-BY_1381]. Normal fault with a throw of up to 40 m.
Gebenbach-Krickelsdorf Fault
Gebenbach-Krickelsdorf Störung
Aus dem 20 m Sprung der Streichlinien abgeleiteter, ostwärts gebogener, SSW-NNE verlaufender Ost-Ast der T-Verzweigung am Nordende der Fensterbach Störung [DE-BY_970], der diese mit der Krickelsdorf-Kainsricht Störung (DE-BY_1381] verbindet, dem westlichsten Ausläufer der Luhe Line [DE-BY_1387].
Inferred from the 20 m drop of contour line, eastward arcuate SSW-NNE trending eastern leg of T junction at the northern termination of Fensterbach Fault [DE-BY_970] linking that with Krickelsdorf-Kainsricht Fault (DE-BY_1381], the westernmost section of Luhe Line [DE-BY_1387].
Gebenbach Fault
Gebenbach Störung
Gebenbacher Störung
WNW-ESE verlaufender West-Ast der T-Verzweigung am Nordende der Fensterbach Störung [DE-BY_970] mit einer Sprunghöhe von bis zu 15 m.
WNW-ESE trending western leg of T junction at the northern termination of Fensterbach Fault [DE-BY_970], featuring a throw of up to 15 m.
Gebenbach-Krondorf Fault
Gebenbach-Krondorf Störung
Krondorfer Störung
Ostwärts gebogen, NNW-SSE verlaufender Zweig des nördlichen Ausläufers der Fensterbach Störung [DE-BY_970], mit einer nach N hin rasch abnehmenden Sprunghöhe von bis zu 130 m.
NNW-SSE trending eastward arcuate branch of the northern tail of Fensterbach Fault [DE-BY_970]. Its throw of up to 130 m rapidly decreases to the north.
Urspring-Lintach Fault
Urspring-Lintach Störung
Urspringer Störung
Gewellt NNW-SSE verlaufende Störung die der Fensterbach Störung [DE-BY_970] entspringt und subparallel zu dieser verläuft.
Undulate NNW-SSE trending fault branching off and running subparallel to Fensterbach Fault [DE-BY_970].
Keilberg Fault System
Keilberg Störungssystem
Mindestens von Büchelkühn S Schwandorf bis nach Regensburg ziehendes, N-S bis NNW-SSE verlaufendes Störungssystem bestehend aus einer östlichen, senkrecht stehenden bis 85° nach ± E einfallenden Aufschiebung mit großer Sprunghöhe und einer westlich subparallelen, steil (85°-60°) nach ± E einfallenden Abschiebung mäßiger Sprunghöhe, mit dazwischenliegenden Grabenstrukturen.
Running at least from Büchelkühn south of Schwandorf to Regensburg, N-S to NNW-SSE trending fault system of an eastern vertical to 85° ± E dipping large throw reverse (step) fault and a subparallel vertical to steeply (85°-60°) ± E dipping moderate throw normal fault, forming a graben structure.
Kreuzbügerl Fault
Kreuzbügerl Störung
Nördliche Fortsetzung der Keilberg Störung [DE-BY_761] nach ihrer Kreuzung mit der Bubach-Maxhütte Störung [DE-BY_1368]. Westwärts gebogene, insgesamt N-S verlaufende, saigere bis subvertikale Abschiebung mit einer Sprunghöhe von höchstens 50 m.
Northern continuation of Keilberg Fault [DE-BY_761] after intersection with Bubach-Maxhütte Fault [DE-BY_1368]. Westward arcuate, overall N-S trending, vertical to subvertical reverse fault with a throw of less than 50 m.
Striessendorf Fault
Striessendorf Querstörung
W-E streichende Querstörung, die den nördlichen Teil der Kreuzbügerl Störung [DE-BY_1370] nach E hin versetzt.
W-E striking lateral fault offsetting the northern section of Kreuzbügerl Fault [DE-BY_1370] to the east.
Büchelkühn-Bubach Fault
Büchelkühn-Bubach Störung
Nördliche Fortsetzung der Bubach-Maxhütte Störung [DE-BY_1368]. N-S streichende, saigere bis subvertikale Abschiebung mit einer Sprunghöhe von höchstens 50 m. Bildet mit der Bubach-Maxhütte Störung [DE-BY_1368] eine flachen Graben.
Northern continuation of Bubach-Maxhütte Fault [DE-BY_1368]. N-S striking, vertical to subvertical normal fault with a throw of less than 50 m, forming a shallow graben with Bubach-Maxhütte Fault [DE-BY_1368].
Bubach-Maxhütte Fault
Bubach-Maxhütte Störung
Gewellt NNW-SSE verlaufende, steil (85°-60°) nach ± E einfallende Abschiebung mit einem Vertikalversatz von etwa 20 m. Bildet mit der östlich parallel verlaufenden Keilberg Störung [DE-BY_761] eine flachen Graben. Vermutete nördliche Fortsetzung der Ponholz-Diesenbach Störung [DE-BY_1367] und, nach ihrer Kreuzung mit der Keilberg Störung [DE-BY_761], im Norden mit der Büchelkühn-Bubach Fault [DE-BY_1369] verbunden.
Undulate NNW-SSE trending, steeply (85°-60°) ± E dipping normal fault featuring a throw of about 20 m, forming a shallow graben with Keilberg Fault [DE-BY_761] paralleling to the east. Inferred northern continuation of Ponholz-Diesenbach Fault [DE-BY_1367] and, after intersecting Keilberg Fault [DE-BY_761], connected to Büchelkühn-Bubach Fault [DE-BY_1369] in its north.
Ponholz-Diesenbach Fault
Ponholz-Diesenbach Störung
Nördliche Fortsetzung der Regental Störung [DE-BY_1243]. Gewellt N-S verlaufende, steil (85°-60°) ± E einfallende Abschiebung parallel zur Keilberg Störung [DE-BY_761].
Northern continuation of Regen Valley Fault [DE-BY_1243] and connectetd to Bubach-Maxhütte Fault [DE-BY_1368] in its north. Undulate N-S trending, steeply (85°-60°) ± E dipping normal fault paralleling Keilberg Fault [DE-BY_761].
Gewellt N-S bis NNW-SSE verlaufende, steil (85°-60°) ± E einfallende Abschiebung zwischen Teublitz und Regensburg. Westgrenze der Grabenstrukturen von Maxhütte und Laub, parallel zur Keilberg-Störung [DE-BY_761].
Undulate N-S to NNW-SSE trending, steeply (85°-60°) ± E dipping normal fault running from Teublitz to Regensburg. Western boundary of the graben structures of Maxhütte and Laub, paralleling Keilberg Fault [DE-BY_761].
Regen Valley Fault
Regental Störung
N-S bis NNW-SSE (eggisch) verlaufende, senkrecht stehende bis 85° nach ± E einfallende Aufschiebung zwischen Teublitz und Regensburg. Westliche Grenze der Böhmischen Masse mit Sprunghöhen bis zu 1,2 km.
N-S to NNW-SSE trending, vertical to 85° ± E dipping reverse fault running from Teublitz to Regensburg. Principal tectonic boundary featuring throws up to 1.2 km, tracing the western limit of the Bohemian Massif.
Keilberg-Sprung
Keilberg Fault
Keilberg-Abbruch
Keilberg Störung
Pittersberg Fault
Pittersberger Störung
Von Freihöls bis Kreith ziehende, leicht gewellt NNW-SSE streichende, steil nach WSW einfallende Aufschiebung der Ostflanke des Pittersberger Sattels auf den Bodenwöhrer Senke. Geht nach SSE hin in eine Flexur und den Pittersberger Sattel über (möglicherweise drapierende Falte in Hangenden der tiefen Störung) und steht wohl mit den nördlichen Ausläufern der Keilberg Störung [DE-BY_761] bzw. Regental Störung [DE-BY_1243] in Verbindung (Bauberger & Streit 1982). Eine Verbindung zur Fensterbach Störung [DE-BY_970] im Norden wird vermutet (Bauberger & Streit 1982), ist aber nicht nachgewiesen.
Running from Freihöls to Kreith, slightly undulate NNW-SSE trending, steeply WSW dipping reverse fault thrusting the eastern slope of the Pittersberg anticline onto the Bodenwöhr Trough. Towards the SSE, passing into a flexure and the southern Pittersberg anticline (possibly a drape fold passively conforming upon the faulted bedrock), the structure probably is connected to the extensions of Keilberg Fault [DE-BY_761] resp. Regen Valley Fault [DE-BY_1243] (Bauberger & Streit 1982). A connection (soft link) with Fensterbach Fault [DE-BY_970] to the north is assumed (Bauberger & Streit 1982) but not evidenced.
Franconian Line
Fränkische Linie
Tektonische Großstruktur an der Grenzlinie der Böhmischen Masse zur Süddeutschen Schichtstufenland, die sich grob NNW-SSE über mehr als 100 km von Stockheimer Becken an der Grenze zu Thüringen bis zur Luhe Line (DE-BY_1387] hinzieht. Auch wenn morphologische deutlich als Abbruch erkennbar, sind ihre nach NE hin einfallenden Auf- und Überschiebungen mit z.T. enormen Vertikalversätzen nur in Abschnitten kartierbar, da von mächtigen Schuttmassen überdeckt, sind geophysikalisch aber nachgewiesen. Nach Zulauf (1991) können die wesentlichen Deformationsphasen der Fränkischen Linie folgendermaßen skizziert werden: Anlage der Fränkischen Linie währen der postvarizischen NE-SW Kompression, dextrale Bewegungen während der N-S Kompression in der Unterkreide, Aufschiebung und Hebung des Grundgebirges auf das Vorland während der alpidischen Gebirgsbildung (Oberkreide bis Paläogen).
Principal tectonic structure of eastern Bavaria, running for more than 100 km roughly NNW-SSE, from Thuringia (entering Bavaria at the Stockheim Rotliegend Trough) on to Luhe Line (DE-BY_1387], separating the Bohemian Massif to the east from the South German Scarpland to the west. Even though physiographically forming a conspicuous scarp, its NE dipping large throw reverse faults are mappable in certain segments only, as covered by thick debris, but are evidenced in geophysical surveys. Main movement stages involving the Franconian Line have been late Variscan NE-SW compression, dextral shearing during Early Cretaceous and the uplift of the Variscan Basement and the overthrust of the foreland during Alpine orogeny (Zulauf 1991).
Klobenreuth-Edeldorf Fault
Klobenreuth-Edeldorf Störung
NW-SE bis NNW-SSE verlaufender Haupt-Ast der Fränkischen Linie zwischen Obersdorf bei Klobenreuth und Edelhof, im nördlichen Teil SW-wärts parallel zur Klobenreuth-Neustadt Störung [DE-BY_1405]. Die beiden Teil-Äste laufen unter dem Waldnaabtal zusammen
NW-SE to NNW-SSE trending main branch of Franconian Line running from Obersdorf near Klobenreuth to Edelhof, in its northwestern part SW-wards parallel to Klobenreuth-Neustadt Fault [DE-BY_1405]. The two branches merge underneath the Waldnaab valley.
Föritz-Pressig Faults
Föritz-Pressig Störungen
Gruppe N-S bis NNW-SSE verlaufender Störungen die die Fränkische Linie nach Süden ablenken und das Stockheimer Becken in Horst- und Graben-artige Schollen zerlegen. Wahrscheinlich bei der Reaktivierung variszischer, NE-SE gerichteter Druckspannungsstrukturen während der dextralen Seitenverschiebung in der Unterkreide in einer Transferzone entstandene Blattverschiebungs­duplexe. In dehnenden Duplexstrukturen entstehen dabei Senken, in denen jüngere Ablagerungen, vor der Erosion geschützt, erhalten bleiben. Diese Strukturen wurden durch die Hebung und Aufschiebung des Grundgebirges auf das Vorland während der Oberkreide und im Paläogen überprägt.
Array of N-S to NNW-SSE trending faults deflecting the direction of Franconian Line to the south, and, by fractionizing Stockheim Basin into subparallel fault-bound horst- and graben-like blocks, separating the crescent-shaped Rotliegend outlier of the trough. Probably strike-slip duplexes of a transfer zone generated by the dextral movement during Early Cretaceous, reactivating the NE-SW compressional structures created while Variscan orogeny. Extensional bends thereby create basins which might expose younger deposits preserved from erosion. These structures have been reshaped as the result of Bohemian Massif uplift and thrust onto the foreland during Late Cretaceous and Paleogene.
Föritz-Stockheim Fault
Föritz-Stockheim Störung
NE-wärts gebogen, insgesamt NNW-SSE verlaufende, nach WSW einfallende Abschiebung; bildet im Süden die Westgrenze des Traindorf Horsts gegen die Stockheimer (Graben-)Scholle.
NE-wards arcuate, overall NNW-SSE trending, WSW dipping normal fault, in its south forming the western boundary of Traindorf Horst towards Stockheim (graben-)block.
Pressig Fault
Pressig Störung
NNW-SSE streichende Aufschiebung mit Einfallrichtung WSW, Ostrand des Spitzberg Horsts gegen die Grossauer (Graben-)Scholle.
NNW-SSE trending reverse fault with dip direction WSW, eastern boundary of Spitzberg Horst towards Grossau (graben-)block.
Welitsch Fault
Welitsch Störung
NNW-SSE streichende Abschiebung mit Einfallrichtung WSW, Westrand des Spitzberg Horsts gegen die Reitscher (Graben-)Scholle.
NNW-SSE trending normal fault with dip direction WSW, western boundary of Spitzberg Horst towards Reitsch (graben-)block.
Stockheim Fault
Stockheim Störung
NNW-SSE streichende Aufschiebung mit Einfallrichtung ENE (abschiebend/strike-slip invertiert). Westliche Begrenzung der Reitscher (Graben-)Scholle gegen den Traindorfer Horst.
NNW-SSE trending reverse fault with dip direction ENE (normal/strike-slip inverted), western boundary of Reitsch (graben-)block towards Traindorf Horst.
Edeldorf-Töglersricht Fault
Edeldorf-Töglersricht Störung
Gewellt NNW-SSE verlaufender, steil bis mäßig steil nach ENE einfallender Haupt-Ast der Fränkischen Linie mit einer Sprunghöhe von bis zu 100 m.
Undulate NNW-SSE trending, steeply to intermediately ENE dipping reverse fault featuring a throw of at least 100 m. Main branch of Franconian Line.
Edeldorf-Almesbach Fault
Edeldorf-Almesbach Störung
Subparallel zur Edeldorf-Töglersricht Störung [DE-BY_1403] NNW-SSE verlaufender westlicher Ast der Fränkischen Linie; trennt Unter-Rotliegend im Westen von Oberkarbon im Osten.
Offsetting Lower Rotliegend in the west from Upper Carboniferous in the east, NNW-SSE trending western branch of Franconian Line running subparallel to Edeldorf-Töglersricht Fault [DE-BY_1403].
Irchenried Fault
Irchenried Störung
Gewellt N-S verlaufender West-Ast der Gleitsbach-Windbühl Störung [DE-BY_1399], der das Unterrotliegend im Westen vom Oberkarbon im Osten abgrenzt.
Undulate N-S trending western branch of Gleitsbach-Windbühl Fault [DE-BY_1399] offsetting Lower Rotliegend in the west from Upper Carboniferous (Pennsylvanian) in the east.
Gleitsbach-Windbühl Fault
Gleitsbach-Windbühl Störung
N-S bis NNW-SSE verlaufende, steil bis mäßig steil nach E einfallende Aufschiebung mit einem Versatz vom mindestens 100 m. Südlichster Abschnitt der Fränkischen Linie [DE-BY_1398] zwischen dem Gleitsbachtal im Norden und der Luhe Störung [DE-BY_965], die sie leicht versetzt, im Süden. Eine Fortsetzung, über die Luhe Störung hinaus, ist wahrscheinlich ("Oberpfalzlineament"), konnte bisher aber nicht nachgewiesen werden (Bauberger 1993).
N-S to NNW-SSE trending, steeply to intermediately E dipping reverse fault featuring a throw of at least 100 m. Southernmost section of Franconian Line [DE-BY_1398] running from Gleitsbach valley in the north to Luhe Fault [DE-BY_965] in the south, slightly displacing Luhe Fault. A continuation beyond Luhe Fault further to the south is probable ("Oberpfalzlineament") but not evidenced yet (Bauberger 1993).
Franconian Forest Scarp
Frankenwald-Randbruch
Frankenwaldrandstörung
Abfolge von grob NW-SE verlaufenden, steil bis flach nach ± NE einfallenden Aufschiebungs-Segmenten am Südwest-Abbruch des Frankenwaldes. Polyphase Aufschiebungen, z.T. in mehrere Teilstörungen aufgespalten, mit einer Gesamt-Sprunghöhe bis über 1 km, wiederholt von kleinräumigen Querstörungen versetzt.
Array of roughly NW-SE trending, steeply to gently ± NE dipping reverse fault segments, forming the southwestern scarp of the Franconian Forest. Polyphase reverse faults, partly split up in subfaults, featuring a (cumulative) throw of up to more than 1 km, repeatedly offset by small-scale lateral faults.
Letzenhof Fault
Letzenhof Störung
WNW-ESE verlaufende, steil nach NNE einfallende Nebenstörung des Frankenwald-Randbruchs. Wird im Osten von der Kronach Störung [DE-BY_993] abgeschnitten und setzt sich im Nordwesten über den Hauptast [DE-BY_1431] hinweg als Welitsch Störung [DE-BY_954] ins Stockheimer Becken fort. Wahrscheinlich, als ehemaliger, prä-Unterkreide-Dextral-Scherung, Hauptast des Frankenwald-Randbruchs, südlicher extensiver Bogen der Blattverschiebungs¬duplexe des Stockheimer Beckens [DE-BY_1428].
WNW-ESE trending, steeply NNE dipping subsidiary fault of Franconian Forest Scarp. Truncated by Kronach Fault [DE-BY_993] to the east and crossing today's main branch [DE-BY_1431], continuing as Welitsch Fault [DE-BY_954] in Stockheim Basin to the northwest. Probably southern extensional bend of the Stockheim Basin strike-slip duplexes [DE-BY_1428] as the pre-Early-Cretaceous-dextral-shearing main branch of the Franconian Forest Scarp.
Leuschberg-Rennesberg Faults
Leuschberg-Rennesberg Verwerfungen
Gruppe NW-SE verlaufender, steil nach SW einfallender Abschiebungen mit einer Sprunghöhe bis zu 200 m, im Bogeninnern der WNW-ESE auf N-S Umlenkung des Frankenwald-Randbruchs bei Zeyern. Möglicherweise Blattverschiebungs­duplexe der dextralen Seitenveschiebung in der Unterkreide, während der die variszischen, NE-SE gerichteten Druckspannungsstrukturen reaktiviert wurden; durch die Hebung und Aufschiebung des Grundgebirges auf das Vorland während der Oberkreide und im Paläogen überprägt und von Querstörungen (z.B. Kronach Störung [DE-BY_993]) versetzt.
Array of NW-SE trending, steeply SW dipping normal faults with a throw up to 200 m, running inwards the NE-ward arcuate Franconian Forest Scarp at Zeyern. Possibly strike-slip duplexes generated by the dextral movement during Early Cretaceous, reactivating the NE-SW compressional structures created while Variscan orogeny. Altered and offset by lateral faults (e.g. Kronach Fault [DE-BY_993]) as a result of Bohemian Massif uplift and thrust onto the foreland during Late Cretaceous and Paleogene.
Sonneberg Fault
Sonneberg Störung
NW-SE verlaufende, nach NE einfallende Aufschiebung; Fortsetzung der Fränkischen Linie auf thüringer Gebiet.
NW-SE trending, NE dipping reverse fault; continuation of Franconian Line on Thuringian territory.
Fichtel Mountains Scarp
Fichtelgebirgs-Randbruch
Fichtelgebirgsrandstörung
NNW-SSE bis WNW-ESE verlaufender mittlerer Abschnitt der Fränkischen Linie zwischen der Müchberger Gneissmasse und der Erbendorfer Linie [DE-BY_1447]. Polyphase Abschiebungssegmente (z.T. als Staffelbruch) mit einer Gesamt-Sprunghöhe bis über 1 km, wiederholt von Querstörungen versetzt, wie z.B. der Muckenreuther Störung [DE-BY_1418].
Veering between a NNW-SSE to WNW-ESE trend, middle segment of Franconian Line running from Münchberg Klippe to Erbendorf Line [DE-BY_1447]. Polyphase reverse fault (or step fault) segments featuring a (cumulative) throw of up to more than 1 km, repeatedly offset by lateral faults such as Muckenreuth Fault [DE-BY_1418].
Fichtelgebirgsrandspalte
Muckenreuth Fault
Muckenreuther Störung
N-S streichende größere Querstörung die den Fichtelgebirgs-Randbruch sinistral versetzt.
N-S striking major lateral fault sinistrally offsetting fault segments of the Fichtel Mountains Scarp.
Föritz Fault
Föritz-Störung
N-S striking normal fault with dip direction E
Altenparkstein Fault
Altenparkstein Störung
SE1 (Seismic Event 1)
Altenparkstein Störungszone
Seismischer Reflektor SE1
Von Waldeck nach Neustadt/Waldnaab ziehende, NW-SE verlaufende, steil bis mäßig nach NE einfallende Aufschiebung subparallel zur Waldeck-Klobenreuth Störungszone [DE-BY_1406]. Nach Markerhorizonten weist die dieser Ast der Fränkischen Line im Bereich der Erbendorfer Linie [DE-BY_1447] einen Vertikalversatz von bis zu 3,5 km auf (Wagner et al. 1997).
NW-SE trending, steeply to intermediately NE dipping reverse fault subparallel to Waldeck-Klobenreuth Fault Zone [DE-BY_1406], running from Waldeck to Neustadt/Waldnaab. Inferred from marker horizons (Wagner et al. 1997) this branch of Franconian Line in the area of Erbendorf Line [DE-BY_1447] features a vertical displacement of up to 3.5 km.
Burggrub Flexure
Burggrub Flexur
Südwestwärts gebogene, N-S bis E-W verlaufende SW-Grenze des Stockheimer Beckens. Flexurartiges "Fehlstück" im Verlauf der von N-S auf E-W drehenden Fränkischen Linie.
SW-wards arcuate N-S to W-E trending SW boundary of Stockheim Basin. Flexure-like "missing link" of the Franconian Line veering from N-S to E-W.
Waldeck-Klobenreuth Fault
Waldeck-Klobenreuth Störung
Waldeck-Klobenreuth Fault Zone
SE2 (Seismic Event 2)
Waldeck-Klobenreuth Störungszone
Seismischer Reflektor SE2
NW-SE trending, intermediately NE dipping reverse fault subparallel to Altenparkstein Fault Zone [DE-BY_1407] running from Waldeck to Obersdorf near Klobenreuth. Inferred from marker horizons (Wagner et al. 1997) this branch of Franconian Line in the area of Erbendorf Line [DE-BY_1447] features a vertical displacement of up to 1.5 km.
Von Waldeck nach Neustadt/Waldnaab ziehende, NW-SE verlaufende, mäßig steil nach NE einfallende Aufschiebung subparallel zur Altenparkstein Störungszone [DE-BY_1407]. Nach Markerhorizonten weist die dieser Ast der Fränkischen Line im Bereich der Erbendorfer Linie [DE-BY_1447] einen Vertikalversatz von bis zu 1,5 km auf (Wagner et al. 1997).
Waldeck Fault
Waldeck Störung
Kurze Abschiebung zwischen der Altenparkstein Störungszone [DE-BY_1407] und Waldeck-Klobenreuth Störungszone [DE-BY_1406].
Short reverse fault in between Altenparkstein Fault Zone [DE-BY_1407] and Waldeck-Klobenreuth Fault Zone [DE-BY_1406].
Klobenreuth-Neustadt Fault
Klobenreuth-Neustadt Störung
NW-SE streichende intra-Basement Nebenstörung der Fränkischen Linie NE-wärts parallel zur Klobenreuth-Edeldorf Störung [DE-BY_1404) zwischen Obersdorf bei Klobenreuth und Neustadt/Waldnaab, wo die Teil-Äste zusammenlaufen.
NW-SE striking intra-basement subfault of Franconian Line running NE-wards parallel to Klobenreuth-Edeldorf Fault [DE-BY_1404] from Obersdorf near Klobenreuth to Neustadt/Waldnaab, where the two branches merge.
Teplá-Barrandian Terrane boundary
Tepla-Barrandium Domänengrenze
Vergleichbar dem Bug eines Eisbrechers ragt die südwestliche Ausbuchtung des in Tschechien großräumig verbreiteten Teplá-Barrandiums am Hohen Bogen östlich vom Cham weit nach Bayern herein. Diese Gabbroamphibolitmasse des Neukirchen-Kdyně-Komplex ist entlang von zwei polyphasen Haupt-Scherzonen auf bzw. in das Moldanubikum s. str. geschoben und endet an einer bogenförmigen Störung im Südwesten. Die als Mylonit-Gürtel ausgebildeten, zum Teplá-Barrandium hin einfallenden Scherzonen weisen eine große Abschiebungskomponente auf: wobei das Teplá-Barrandium ggü. dem Moldanubikum um einen Vertikalversatz von über 10 km abgesenkt ist (Bues et al. 1998, Zulauf et al. 2002).
Comparable to the ship's bow of an icebreaker the southwestern bulge of Teplá-Barrandian Terrane, widespread in Czechia, protrudes into Bavarian territory east of Cham. The Gabbroamphibolite body of Neukirchen-Kdyně-Complex is thrusted into the Moldanubian s. str. along two principal polyphase shear zones, headed by an arched thrust front in the southwest. These thrust zone have been subject to dip-slip or oblique-slip normal movements, moving down the Teplá-Barrandian unit with respect to the Moldanubian unit for more than 10 km, forming mylonite belt, dipping steeply towards the Teplá-Barrandian unit (Bues et al. 1998, Zulauf et al. 2002).
Krušné hory Fault
The Eger Graben northern marginal rift fault (Krušné hory Fault) is regarded a normal fault, conjugate to the southern marginal rift fault. Formed during the Cenozoic in several (reactivation) phases and due to the uplift of Krušné hory mountains block in Pliocene/Pleistocene, after the rift formation, it features a present day residual throw of more than 700 m.
Eger Graben Northern Marginal Rift Fault
Egergraben Nordrand- Verwerfung
Hoher Bogen Shear Zone
Hoher Bogen Scherzone
HBSZ
Bogenförmige Stirn des Neukirchen-Kdyně Komplex. Steil nach ± NE einfallende Störung, zunächst Auf-/Überschiebung, danach (Rückgleite-) Abschiebung, als Verbindung zwischen der rechtssinnigen Westböhmischen Scherzone [DE-BY_1353] und der linkssinnigen Zentralböhmischen Scherzone [DE-BY_1354].
Frontal arch of the Neukirchen-Kdyně Complex Boundary. Steeply ± NE dipping initially reverse (“on-thrust”) fault, then inverted to a normal (“back-slip”) fault, connecting dextral West Bohemian Shear Zone [DE-BY_1353] and sinistral Central Bohemian Shear Zone [DE-BY_1354].
Hoher Bogen lateral faults
Hoher Bogen Querstörungen
NNW-SSE to NNE-SSW trending faults within Neukirchen-Kdyně-Complex.
Central Bohemian Shear Zone
Zentralböhmische Scherzone
CBSZ
Klattauer Störung
Undulate WSW-ENE trending sinistral shear zone forming the southeastern Boundary of the Gabbroamphibolite body of Neukirchen-Kdyně-Complex of the Teplá-Barrandian Zone.
Gewellt WSW-ENE verlaufende linkssinnige Scherzone als südöstliche Begrenzung der Gabbroamphibolitmasse des Neukirchen-Kdyně-Komplex im Teplá-Barrandium.
CBSZ subsidiary faults
CBSZ Nebenstörungen
WSW-ENE verlaufende linkssinnige Blatt- oder Schrägabschiebungen subparallel zur Zentralböhmischen Scherzone [DE-BY_1354).
WSW-ENE trending subsidiary sinistral strike-slip or oblique-slip faults subparallel to Central Bohemian Shear Zone [DE-BY_1354].
Tachov Fault Zone
Böhmischer Pfahl
Bohemian Quartz Lode
Overall NNW–SSE trending Tachov Fault presumably runs for more than 120 km from Aš NW of Cheb to HBSZ [LfU-BY_1355]. In the southern part, Tachov Fault Zone (TFZ), a wide belt of prevailing mylonites, is a synonym for West Bohemia Shear Zone (WBSZ) [LfU-BY_1353], and associated with quartz lodes, thus also referred to as Bohemian Quartz Lode or Bohemian Pfahl. Here, the western boundary of TFZ consists of a set of (sub-)parallel zones of the Bohemian Quartz Lode between the eastern suture-type Tachov Fault s.str. and the western Nemanice-Rozvadov Fault, both steeply ENE dipping to vertical polyphase dextral oblique-slip normal faults (Zulauf et al. 2002). In its central and southern sections, Tachov Fault represents the western flank of Cheb-Domažlice Graben (aka Cheb Basin / Chebská pánev / Egerer Becken and Tachov Trough / Tachovská brázda / Tachauer Furche).
Tachov Fault Zone subsidiary faults
TFZ Nebenstörungen
Böhmischer Pfahl Störungen
NNW-SSE to N-S trending subsidiary dextral strike-slip or oblique-slip faults subparallel to Tachov Fault Zone [LfU-BY_9920], partly manifested as quartz lodes and pegmatite veins.
The trends and geometries of Tachov Fault Zone subsidiary faults are represented schematically only.
Mariánské Lázně Fault Zone
Marienbader Störungszone
MLZ
About 150 km long, prevailing NNW-SSE trending, morphologically conspicuous, principal tectonic structure in western Bohemia. Limit of several distinctive geological units of the Bohemian Massif: Saxothuringian Zone in the NW, Moldanubian s. str. in the S and SW, Teplá-Barrandian Block in the E and truncating Eger Graben. In its S, eastern boundary of Cheb-Domažlice Graben (Tachovská brázda /Tachauer Furche). The merger, respectively cross-over, of Mariánské Lázně Fault Zone with N-S striking Počatky-Plesná Fault Zone at Nový Kostel north of the Eger Graben is recurrently prone to earthquake swarms with a hypocenter at about 10 km, inferred to be caused by channeled ascent of fluids along the fault plane in the crust.
Litoměřice / Ohře Fault
Egergraben Südrand-Verwerfung
Eger Graben Southern Marginal Rift Fault
The southern marginal rift fault (Litoměřice / Ohře Fault) is the surface outcrop of the deep-seated Litoměřice Fault, interpreted as a Variscan suture between the Saxothuringian and Tepla-Barrandian/Moldanubian zones, reactivated in Cenozoic times due to Alpine orogeny. This North Bohemian Sher Zone (NBSZ) is considered the original forming structure of the entire rift, composed of wide zone of (sub-)parallel faults and en-echelon structures.
West Bohemian Shear Zone
Westböhmische Scherzone
WBSZ
Von der Mariánské Lázně Störung bzw. dem Bor Granit bis zur HBSZ [DE-BY_1355] verlaufende, N-S bis NNW-SSE streichende, rechtssinnige Scherzone als westliche Begrenzung der Gabbroamphibolitmasse des Neukirchen-Kdyně-Komplex im Teplá-Barrandium. Die Hauptbewegungsphasen umfassen die NE-wärts einfallende Abschiebung vor ca. 360 Ma und die dextrale Seiten- bzw. Schrägabschiebung vor ca. 340 Ma (Zulauf et al. 2002).
Running from Mariánské Lázně Fault resp. Bor granite to HBSZ [DE-BY_1355], N-S to NNW-SSE trending oblique-slip normal shear zone (main kinematic phases: NE dipping normal fault roughly 360 Ma ago, dextral shearing approx. 340 Ma ago (Zulauf et al. 2002)) forming the western boundary zone of Neukirchen-Kdyně-Complex of the Teplá-Barrandian Zone.
WBSZ subsidiary faults
WBSZ Nebenstörungen
NNW-SSE bis NNE-SSW verlaufende, dextrale Blatt- oder Schrägabschiebungen subparallel zur oder in der Verlängerung der Westböhmischen Scherzone [DE-BY_1353), z.T. als Quarz- und Pegmatit-Gänge.
NNW-SSE to NNE-SSW trending subsidiary dextral strike-slip or oblique-slip faults subparallel to or extending West Bohemian Shear Zone [DE-BY_1353], partly manifested as quartz and pegmatite veins.
West Bohemian Shear Zone (CZ)
N-S to NNW-SSE trending eastern strand of WBSZ s.l., aka Bohemian Pfahl, running subparallel Tachov Fault Zone [LfU-BY_9920]. Eastern part of the stepped normal oblique-slip shear zone, main kinematic phases: NE dipping normal fault roughly 360 Ma ago, dextral shearing approx. 340 Ma ago (Zulauf et al. 2002), forming a ductile normal faulting shear zone.
1: Tectonic Boundary Objects in the central part of the North Alpine Molasse Basin and northward adjoining areas
Tektonische Grenzflächen im mittleren Teil des Nordalpinen Molassebeckens und nördlich angrenzender Gebiete
Concepts of tectonic boundaries in the Central North Alpine Molasse Basin, in terms of fault traces in the Upper Jurassic carbonates hydrothermal reservoir and hydraulically connected northward adjoining realms of outcropping reservoir rocks of the Swabian and Franconian Alb. Synopsis of basinal blind faults, predominantly interpreted from seismic surveys of various vintage and resolution or derived from borehole correlation in shallower marginal areas, as well as mapped superficial faults in exposed areas. This inventory, prepared within the scope of HotLime project case study 1, comprises tectonic boundaries in Baden-Wuerttemberg [DE-BW] and Upper Austria [AT] as well.
Konzepte tektonischer Grenzflächen im zentralen nordalpinen Molassebecken, bezogen auf die Schnittspuren in den oberjurassischen Karbonaten des hydrothermalen Reservoirs, sowie den zu Tage tretenden Reservoirgesteinen in nördlich angrenzenden Bereichen, der Schwäbisch-Fränkischen Alb. Zusammenstellung der überdeckten Störungen im Becken, basierend auf der Interpretation seismischer Erkundungen aus fünf Jahrzehnten und mit unterschiedlicher Auflösung, oder abgeleitet aus Bohrloch-Korrelationen in seichteren Randbereichen, sowie kartierten Störungen im Ausstrichbereich. Dieses Inventar wurde im Rahmen des Projekts HotLime, Pilotgebiet 1, erstellt und umfasst auch tektonische Grenzflächen in Baden-Württemberg [DE-BW] und Oberösterreich [AT].
Lower Bavaria - Upper Austria Molasse Basin fault domain
All faults of the Lower Bavaria - Upper Austria Molasse Basin are blind faults 3D modelled based on evidence of seismic and gravity surveys and deep drillings. The concepts refer to the fault traces on the top of Upper Jurassic carbonate sequence as one of the principal reflectors in seismic surveys. Tectonic boundaries featuring throws of less than approximately 10 m, likewise soft links between faults, like relay ramps or horsetail splays, commonly are subseismic in legacy surveys and detectable only in novel 3D-seismics as carried out in few focus areas. The inventory, thus, cannot be complete with respect to these features, reflects the state of knowledge as of 2020 and is subject to future amendments.
Alle Störungen im niederbayerisch-oberösterreichischen Molassebecken sind überdeckte Störungen, die im 3D-Modell aus seismischen und Schwere-Messungen sowie Bohrungsbelegen abgeleitet wurden. Die Konzepte der tiefliegenden Störungen beziehen sich auf die im 3D-Modell ermittelten Schnittspuren an der Oberfläche der Weißjura Karbonat-Abfolge. Tektonische Grenzflächen mit Sprunghöhen von weniger als ca. 10 m, gleichermaßen Übergänge zwischen Störungen wie Relais Rampen (relay ramps) oder Auffiederungen (horsetail splays), sind in älteren seismischen Erkundungen gemeinhin nicht erkennbar (subseismisch) und nur in moderner, in wenigen Schwerpunktbereichen durchgeführter 3D-Seismik identifizierbar. Dementsprechend bleibt die Zusammenstellung, Stand 2020, im Hinblick auf solche Phänomene unvollständig und ist Gegenstand künftiger Fortschreibungen.
Niederbayerisch-oberösterreichisches Molassebecken Störungs-Domäne
The Lower Bavaria - Upper Austria Molasse Basin fault domain, overlapping the Austrian-German border, takes up the space in-between the southwestern scarp of the buried Landshut-Neuötting crystalline rise or Central Swell Zone to the southwest, the Franconian Alb to the northwest, the outcropping crystalline rock suites of the Bohemian Massif to the north and northeast, and the Alpine Thrust front to the south. It is characterized by syn- and antithetic normal faults running subparallel to the counterfort of the Alpine thrust formed by the Bohemian Massif, southwards increasingly crossed by faults subparallel to the Alpine Thrust Front. The roughly NW-SE trending (Variscan strike) reactivated Permo-Carboniferous lineaments subdivide specifically the Lower Bavaria Molasse Basin into sub-basins and troughs. All faults within the basin are blind faults, active until Badenian of mid-Miocene at the latest, solely evidenced by seismic surveys and drillings.
Das niederbayerisch-oberösterreichische Molassebecken wird begrenzt durch den südwestlichen Abbruch des überdeckten Kristallins im Landshut-Neuöttinger Hoch bzw. der Zentralen Schwellenzone im Südwesten, die Fränkische Alb im Nordwesten, die anstehenden Kristallingesteine der Böhmischen Masse in Norden und Nordosten sowie die Alpine Überschiebungsfront im Süden. Für dieses Teilbecken sind syn- und antithetische Abschiebungen subparallel zur Böhmischen Masse, dem Widerlager des Alpenschubs, kennzeichnend, die nach Süden hin zunehmend von Alpenfront-parallelen Störungen überlagert werden. Die grob NW-SE (herzynisch) verlaufenden, reaktivierten permokarbonischen Lineamente untergliedern insbesondere das Niederbayerische Molassebecken in Teilbecken und Tröge. Alle Störungen innerhalb des Beckens sind überdeckte Störungen, die bis höchstens ins Badenium (mittleres Miozän) aktiv waren und nur durch seismische Untersuchungen und Bohrungen nachgewiesen sind.
Haunersdorf-Perbing Fault
Haunersdorf-Perbing Störung
W-E striking, approx. 85° S dipping synthetic normal fault running south of and subparallel to Vils river SE of Landau / Isar.
W-E streichende, ca. 85° nach S einfallende synthetische Abschiebung südlich und subparallel zur Vils SE von Landau / Isar.
Landshut-Neuötting Step Fault
Landshut-Neuötting fault scarp
Landshut-Neuöttinger Abbruch
Landshut-Neuötting Abbruch
NW-SE trending step fault system of steeply SW dipping to vertical normal faults of hercynian (variscan) origin and Miocene reactivation. Southwestern boundary of Landshut-Neuötting crystalline rise, a tilted, gently northeast sloping fault-block featuring an only thin and discontinuous Mesozoic overburden resting upon the basement rocks.
NW-SE (herzynisch) streichender, während der saxonischen Bruchtektonik angelegter, im Miozän reaktivierter Staffelbruch steil nach SW einfallender, bereichsweise vertikaler Abschiebungen. Südwestliche Begrenzung des Landshut-Neuöttinger Hochs, einer nach Nordosten hin flach abtauchenden Kippscholle, in deren Hochgebieten die mesozoische Auflage nur geringmächtig ausgebildet ist und bereichsweise fehlt.
Landshut-Neuötting Fault Scarp 2
Landshut-Neuötting Abbruchstufe 2
Central scarp of Landshut-Neuötting Step Fault [DE-BY_700]. Undulate overall NW-SE trending, averaged approx. 70° SW dipping synthetic normal fault, running from Rudelzhausen to the Austrian Border near Burghausen and beyond.
Mittlere Bruchstufe des Landshut-Neuötting Abbruchs [DE-BY_700], die sich von Rudelzhausen bis zur österreichischen Grenze bei Burghausen und darüber hinaus erstreckt. Gewellt, insgesamt NW-SE verlaufende, im Mittel ca. 70° nach SW einfallende synthetische Abschiebung.
Münchsdorf Fault
Münchsdorf Störung
Subordinate scarp of Landshut-Neuötting Step Fault [DE-BY_700] close and parallel to Landshut-Neuötting Fault Scarp 2 [DE-BY_702]. Probably due to a mostly subseismic throw traceable in a short segment only.
Untergeordnete Bruchstufe des Landshut-Neuötting Abbruchs [DE-BY_700] parallel zur Abbruchstufe 2 [DE-BY_702]. Wahrscheinlich bedingt durch einen überwiegend subseismischen Versatz nur in einem kurzen Abschnitt nachweisbar.
Landshut-Neuötting Main Scarp
Landshut-Neuötting Abbruchstufe 1
Landshut-Neuötting Hauptabbruch
Nordöstliche und größte Bruchstufe des Landshut-Neuötting Abbruchs [DE-BY_700], die sich von Volkenschwand bis zur österreichischen Grenze bei Burghausen und darüber hinaus erstreckt. Gewellt, insgesamt NW-SE verlaufende, im Mittel ca. 85° nach SW einfallende synthetische Abschiebung.
Northeastern and principal scarp of Landshut-Neuötting Step Fault [DE-BY_700]. Undulate overall NW-SE trending, on average approx. 85° SW dipping synthetic normal fault, running from Volkenschwand to the Austrian Border near Burghausen and, as Handenberg Fault [AT_10655] further into Austrian territory.
Volkenschwand Fault
Volkenschwand Störung
N-S striking, steeply (85°-60°) W dipping normal fault. Lateral fault of Landshut-Neuötting Main Scarp, western boundary of a horst-like structure, confined by Furth Fault [DE-BY_705] to the east, lacking Upper Jurassic deposits on top of the crystalline basement.
N-S streichende steil (85°-60°) nach W einfallende Abschiebung. Querstörung zum Landshut-Neuötting Hauptabbruch. Bildet mit der Furth Störung [DE-BY_705] eine Horst-artige Struktur, in der Oberjura als Grundgebirgsüberdeckung fehlt.
Furth Fault
Furth Störung
N-S striking, steeply (85°-60°) E dipping normal fault. Lateral fault of Landshut-Neuötting Main Scarp, eastern boundary of a horst-like structure, confined by Volkenschwand Fault [DE-BY_706] to the west, lacking Upper Jurassic deposits on top of the crystalline basement.
N-S streichende, steil (85°-60°) nach E einfallende Abschiebung. Querstörung zum Landshut-Neuötting Hauptabbruch. Bildet mit der Volkenschwand Störung [DE-BY_706] eine Horst-artige Struktur, in der Oberjura als Grundgebirgsüberdeckung fehlt.
Landshut Fault
Landshut Störung
N-S striking, vertical to subvertical normal fault. Lateral fault of Landshut-Neuötting Main Scarp.
N-S streichende, ± senkrecht stehende Abschiebung. Querstörung zum Landshut-Neuötting Hauptabbruch.
Perach Fault
Perach Störung
NW-SE striking, vertical to steeply SW dipping reverse fault northeastward subparallel to Landshut-Neuötting Main Scarp [DE-BY_701] north of Burghausen.
NW-SE verlaufende, senkrecht stehende bis steil nach SW fallende Aufschiebung nordöstlich subparallel zum Landshut-Neuötting Hauptabbruch [DE-BY_701] nördlich von Burghausen.
Landshut-Neuötting Fault Scarp 3
Landshut-Neuötting Abbruchstufe 3
Southwestern scarp of Landshut-Neuötting Step Fault [DE-BY_700] running from Tattendorf south of Vilsbiburg to Altötting. Undulate overall NW-SE trending, averaged approx. 70° SW dipping synthetic normal fault.
Südwestliche Bruchstufe des Landshut-Neuötting Abbruchs [DE-BY_700], die sich von Altfraunhofen S Landshut bis zur österreichischen Grenze und darüber hinaus erstreckt. Gewellt, insgesamt NW-SE verlaufende, im Mittel ca. 70° nach SW einfallende synthetische Abschiebung.
Rotthalmünster Fault
Rotthalmünster Störung
W-E striking, approx. 85° S dipping synthetic normal fault running from Kirn to Birnbach-Füssing Step Fault [DE-BY_930].
Von Kirn bis zum Birnbach-Füssinger Abbruch [DE-BY_930] verlaufende, W-E streichende, ca. 85° nach S einfallende synthetische Abschiebung.
Stubenberg-Malching Fault
Stubenberg-Malching Störung
W-E striking, approx. 70° S dipping synthetic normal fault.
W-E streichende, ca. 70° nach S einfallende synthetische Abschiebung.
Gumpersdorf-Schellenberg Fault
Gumpersdorf-Schellenberg Störung
WSW-ENE striking, approx. 85° NNW dipping antithetic normal fault north of Simbach am Inn
WSW-ENE streichende, ca. 85° nach NNW einfallende antithetische Abschiebung nördlich von Simbach am Inn.
Schierling Fault
Schierling Störung
Die WNW-ESE streichende, im Mittel ca. 70° nach SSW einfallende synthetische Abschiebung verläuft im Molasseuntergrund von Hausen via Schierling bis Landau/Isar.
The WNW-ESE striking synthetic normal fault runs at the Molasse subsurface from Hausen via Schierling to Landau/Isar. At average, it dips towards approx. 70° SSW.
Schierling-Störung
Landau Fault
Landau Störung
SSW-NNE striking, approx. 85° ESE dipping to vertical synthetic normal fault.
SSW-NNE streichende, ca. 85° nach ESE einfallende bis saigere synthetische Abschiebung.
Wurmannsquick-Zeilarn Fault
Wurmannsquick-Zeilarn Störung
NW-SE trending, approx. 85° NE dipping reverse fault south of Eggenfelden.
NW-SE verlaufende, ca. 85° nach NE einfallende Aufschiebung südlich Eggenfelden.
Hirschbach Fault
Hirschbach Störung
Northward arcuate W-E trending, approx. 70° N dipping antithetic normal fault running from Pfarrkirchen to Grottham north of Bad Birnbach.
Nordwärts gebogen W-E verlaufende, ca. 70° nach N einfallende antithetische Abschiebung zwischen Pfarrkirchen und Grottham nördlich Bad Birnbach.
Dingolfing Fault
Dingolfing Störung
Running from Herrngiersdorf to Marklkofen, NW-SE trending, averaged approx. 70° ± SW dipping normal fault.
NW-SE verlaufende, im Mittel ca. 70° nach ± SW einfallende Abschiebung zwischen Herrngiersdorf und Marklkofen.
Abensberg-Rottenburg Fault
Abensberg-Rottenburg Störung
Northeastward arcuate NW-SE trending, steeply (85°-60°) SW dipping synthetic normal fault.
Nordostwärts gebogen NW-SE verlaufene, steil (85°-60°) nach SW einfallende synthetische Abschiebung.
Holzhamm-Lanzing Fault
Holzhamm-Lanzing Störung
WSW-ENE striking, approx. 85° NNW dipping antithetic normal fault north of Pfarrkirchen.
WSW-ENE streichende, ca. 85° nach NNW einfallende antithetische Abschiebung nördlich von Pfarrkirchen.
Rottenburg-Aham Fault
Rottenburg-Aham Störung
WNW-ESE to NW-SE trending, predominantly vertical normal fault.
WNW-ESE bis NW-SE verlaufende, überwiegend senkrecht stehende Abschiebung.
Jägerndorf-Schwarzenstein Fault
Jägerndorf-Schwarzenstein Störung
NW-SE striking, approx. 85° NE dipping antithetic normal fault between Arnstorf and Pfarrkirchen.
NW-SE streichende, ca. 85° nach NE einfallende antithetische Abschiebung zwischen Arnstorf und Pfarrkirchen.
Hohenthann-Wolkersdorf Fault
Hohenthann-Wolkersdorf Störung
NW-SE trending steeply SW dipping to vertical normal fault.
NW-SE (herzynisch) verlaufende, steil nach SW einfallende bis vertikale Abschiebung.
Jägerndorf-Holzhamm Fault
Jägerndorf-Holzhamm Störung
N-S striking, approx. 80° E dipping antithetic normal fault between Arnstorf and Pfarrkirchen.
N-S streichende, ca. 80° nach E einfallende antithetische Abschiebung zwischen Arnstorf und Pfarrkirchen.
Regensburg-Straubing Trough SW Fringe
Linear array of roughly NW-SE trending, steeply ± NE dipping normal faults, southwestern limit of Regensburg-Straubing Trough.
Regensburg-Straubinger Senke SW Rand
Abfolge von etwa NW-SE verlaufenden, steil nach ± NE einfallender Abschiebungen die den südwestlichen Rand der Regensburg-Straubinger Senke bilden.
Oberschneiding Transverse Fault
Oberschneiding Querstörung
WSW-ENE striking, approx. 85° NNW dipping to vertical antithetic normal fault linking Hagelstadt-Oberschneiding Fault [DE-BY_931] and Pfarrkirchen Fault [DE-BY_763].
WSW-ENE streichende, ca. 85° nach NNW einfallende bis saigere antithetische Abschiebung als Verbindung von Hagelstadt-Oberschneiding Störung [DE-BY_931] and Pfarrkirchen Störung [DE-BY_763].
Köfering Fault
Köfering Störung
WNW-ESE striking, approx. 70° NNE dipping normal fault running from Hohengebraching to Moosham.
WNW-ESE streichende, ca. 70° nach NNE einfallende Abschiebung zwischen Hohengebraching und Moosham.
Hagelstadt-Oberschneiding Fault
Hagelstadt-Oberschneiding Störung
NW-SE striking, approx. 70° NE dipping antithetic normal fault running from Hagelstadt to Oberschneiding. Offset northeastwards by Oberschneiding Transverse Fault [DE-BY_923] it continues to Simbach as Pfarrkirchen Fault [DE-BY_ 763] and further into Austrian territory.
NW-SE streichende, ca. 70° nach NE einfallende synthetische Abschiebung zwischen Hagelstadt und Oberschneiding. Nordostwärts versetzt durch die Oberschneiding Querstörung [DE-BY_923], setzt sie sich als Pfarrkirchen Störung [DE-BY_763] nach Simbach und weiter nach Österreich fort.
In the Swabian-Franconian Alb, evidencing of tectonic boundaries is aggravated by small scale facies changes in the carbonate rocks, including a massive facies, which does not allow contouring of stratification. The concepts of tectonic boundaries in the Swabian-Franconian Alb are thus based on extrapolations on strike of short segments of mapped faults and/or derived from offsets, mismatches or narrowing intervals of contour lines, inferred from borehole correlation or the survey of lineaments. Except for the direct observation these methods are rather imprecise with respect to the dip angle, which, hence, have to be considered a rough estimate.
In der Schwäbisch-Fränkischen Alb wird der Nachweis tektonischer Grenzflächen durch rasche Fazieswechsel der Karbonatgesteine, darunter Massenfazies, die keine Konstruktion von Streichlinien erlaubt, erschwert. Die Konzepte tektonischer Grenzlinien der Schwäbisch-Fränkischen Alb basieren daher auf der Extrapolation kurzer Abschnitte kartierter Störungen im Streichen und/oder sind aus dem Versatz oder dem Zusammenlaufen von Streichlinien abgeleitet, oder beruhen auf Bohrloch-Korrelationen. Genaue Einfallswinkel der Störungen lassen sich daraus nur selten Ableiten; diese Angaben sind daher nur als grobe Schätzung zu betrachten.
The Swabian-Franconian Alb is made up of Upper Jurassic carbonate rocks forming the uppermost cuesta of the South German Scarpland, the Southern Cuesta Terrain. In its major part, the elongated, SW-NE trending ridge overlapping the territories of Baden-Württemberg and Bavaria forms a gently SE dipping platform submerging underneath the Tertiary sedimentary sequence of the Molasse Basin. In its east, except for the faults and flexures relatable to the Schwarzwald-Bayerwald Line [DE-BY_1255] no prevailing tectonic structures are conspicuous. The predominant strike directions of micro-tectonics SSW-NNE (Rhenish) and SE-NW (Variscan / Hercynian) are evidenced by the fault network in few areas only, however, in the west, are manifested in local graben structures. The most striking structural feature of Swabian-Franconian Alb is atectonic: the almost circular crater rim of the 14.6 Ma old Ries asteroid impact.
Die Schwäbisch-Fränkische Alb wird von oberjurassischen Karbonatgesteinen aufgebaut, die die oberste Schichtstufe des Süddeutschen Schichtstufenlands, das Südliche Schichtstufenland bilden. Der SW-NE verlaufende, langgesteckte Höhenzug der Schwäbischen und südlichen Fränkischen Alb, der Gebiete in Baden-Württemberg und Bayern einnimmt, bildet grob betrachtet eine schräggestellte, nach leicht SE einfallende Gesteinsplatte, die nach Süden hin unter die Tertiärablagerungen des Molassebeckens abtaucht. Mit Ausnahme der Störungen und Flexuren die der Schwarzwald-Bayerwald Linie [DE-BY_1255] zugeschrieben werden, sind im Osten (Fränkische Alb) keine übergeordneten tektonischen Strukturen erkennbar. Die vorherrschenden Kluftrichtungen, rheinisch (SSW-NNE) und herzynisch (NW-SE), zeigen sich nur bereichsweise in Störungsnetzwerk, manifestieren sich aber im Westen (Schwäbische Alb) in lokalen Grabenstrukturen. Das auffälligste Strukturelement der Schwäbisch-Fränkischen Alb ist atektonisch: der fast kreisrunde Kraterrand des Ries Asteroideneinschlags vor 14,6 Mio. Jahren.
Schwäbisch-Fränkische Alb Störungs Domäne
Swabian-Franconian Alb fault domain
WSW-ENE streichende, nach SSE einfallende Abschiebung mit unbekanntem Einfallswinkel.
[geola_012]
WSW-ENE striking normal fault, dipping SSE with unknown angle
In der Freiburg-Bonndorf-Bodensee Störungszone, als Nordteil der Südschwarzwald-Dinkelberg-Hegau Störungs-Region, treten NW-SE streichende Elemente in den Vordergrund. Wegen des Höhenversatzes werden die Strukturen meist als tektonische Gräben und Horste dargestellt, doch zeigen Harnischflächen und Herdflächenlösungen rezenter Erdbeben rechtslaterale (NW-SE Brüche) bzw. linkslaterale (SSW-NNE Brüche) Bewegungen. Die vertikalen Sprunghöhen sind diesen Horizontalbewegungen offenbar nachgeordnet.
Freiburg-Bonndorf-Lake Constance Fault Zone
Freiburg-Bonndorf-Bodensee Störungszone
Within the Freiburg-Bonndorf-Lake Constance Fault Zone, as the northern part of the Southern Black Forest-Dinkelberg-Hegau Fault Domain, NW-SE trending features prevail. Due to their significant vertical throw the tectonic boundaries mostly are assigned to horst and graben structures, however, slickenside surfaces and hypocenter retracing of recent earthquakes show dextral (for NW-SE faults) and sinistral (for SSW-NNE faults) movements, obviously superordinate to the vertical throw.
Freiburg-Bonndorf-Lake Constance Fault 1
NW-SE streichende, nach SW einfallende Abschiebung mit unbekanntem Einfallswinkel.
Freiburg-Bonndorf-Bodensee Störung 1
NW-SE striking normal fault, dipping SW with unknown angle
Bonndorfer Störungszone
Bonndorf Fault Zone
Predominantly NW-SE to WNW-ESE striking dextral strike-slip faults with a subordinate vertical movement (oblique slip).
Überwiegend NW-SE bis WNW-ESE verlaufende, rechtssinnige Blattverschiebungen mit untergeordnetem vertikalen Versatz.
WNW-ESE streichende Blattverschiebung; NW-SE bis NNW-SSE streichende Abschnitte als Abschiebung Richtung NNE mit unbekanntem Einfallswinkel ausgeprägt.
WNW-ESE trending strike-slip fault; NW-SE to NNW-SSE striking parts as normal faults dipping NNE with unknown angle
Bonndorf Zone Fault 9
Bonndorfer Störungszone Verwerfung 9
NW-SE striking strike-slip fault
NW-SE streichende Blattverschiebung.
Bonndorf Zone Fault 2
Bonndorfer Störungszone Verwerfung 2
WNW-ESE streichende Blattverschiebung.
WNW-ESE striking strike-slip fault
Bonndorfer Störungszone Verwerfung 1
Bonndorf Zone Fault 1
Bonndorf Zone Fault 4
Bonndorfer Störungszone Verwerfung 4
Bonndorf Zone Fault 3
Bonndorfer Störungszone Verwerfung 3
Bonndorfer Störungszone Verwerfung 6
Bonndorf Zone Fault 6
Bonndorf Zone Fault 5
Bonndorfer Störungszone Verwerfung 5
Bonndorf Zone Fault 8
WSW-ENE striking strike-slip fault
WSW-ENE streichende Blattverschiebung.
Bonndorfer Störungszone Verwerfung 8
Bonndorf Zone Fault 7
Bonndorfer Störungszone Verwerfung 7
Freiburg-Bonndorf-Lake Constance Fault 2
Freiburg-Bonndorf-Bodensee Störung 2
WNW-ESE streichende, nach NNE einfallende Abschiebung mit unbekanntem Einfallswinkel.
WNW-ESE striking normal fault, dipping NNE with unknown angle
Freiburg-Bonndorf-Lake Constance Fault 3
Freiburg-Bonndorf-Bodensee Störung 3
W-E streichende, nach S einfallende Abschiebung mit unbekanntem Einfallswinkel.
W-E striking normal fault, dipping S with unknown angle
[geola_011]
SSW-NNE striking normal fault, dipping ESE with unknown angle
SSW-NNE streichende, nach ESE einfallende Abschiebung mit unbekanntem Einfallswinkel.
The roughly triangular area between Lörrach, Denzlingen and Konstanz is clearly separated from the Upper Rhine Rift as well as from the Upper Swabian Molasse Basin and the Southern Cuesta Terrain due to its structural division. It is the most uplifted and tilted area in Baden-Württemberg. The region between the southern Upper Rhine Graben and Lake Constance is intensively structured by fractures trending NW -SE and SSW-NNE with a height offset between a few meters and almost 200 m. In the north of the area (southern Black Forest-Randen-Hegau), within the Freiburg-Bonndorf-Lake Constance fault zone, the NW-SE trending elements come to the fore while in the south (Dinkelberg, High Rhine, continued in the Table Jura) the SSW-NNE trending elements are more prominent, without completely displacing the other. Because of the significant offset, the structures are mostly represented as tectonic graben and horst structures, but slickenside surfaces and displacements at rupture surfaces from recent earthquakes show right-lateral (NW-SE) or left-lateral (SSW-NNE fractures) movements. The throw of faults are obviously subordinate to these horizontal movements and possibly secondary compensatory movements due to the bulging and tilting of the crust between the Jura and Upper Rhine Rifts.
Südschwarzwald-Dinkelberg-Hegau Region Störungen
Das etwa dreieckige Gebiet zwischen Lörrach, Denzlingen und Konstanz ist durch seine strukturelle Gliederung sowohl gegen den Oberrheingraben als auch gegen das oberschwäbische Molassebecken und das Südliche Schichtstufenland deutlich abgesetzt. Es handelt sich um das am stärksten gehobene und verkippte Gebiet in Baden-Württemberg. Die Region zwischen südlichem Oberrheingraben und Bodensee ist intensiv durch NW-SE- und SSW-NNE-streichende Brüche mit einem Höhenversatz zwischen wenigen Metern und annähernd 200 m gegliedert. Im Norden des Gebiets (Südschwarzwald–Randen–Hegau) treten dabei in der Freiburg–Bonndorf–Bodensee-Störungszone die NW-SE-, im Süden (Dinkelberg, Hochrhein, fortgesetzt im Tafeljura) die SSW-NNE-streichenden Elemente in den Vordergrund, ohne die jeweils anderen ganz zu verdrängen. Wegen des Höhenversatzes werden die Strukturen meist als tektonische Gräben und Horste dargestellt, doch zeigen Harnischflächen und Herdflächenlösungen rezenter Erdbeben rechtslaterale (NW-SE-) bzw. linkslaterale (SSW-NNE-Brüche) Bewegungen. Die vertikalen Sprunghöhen sind diesen Horizontalbewegungen offenbar nachgeordnet und möglicherweise sekundäre Ausgleichsbewegungen infolge der Aufwölbung und Verkippung der Kruste zwischen Faltenjura und Oberrheingraben.
Südschwarzwald-Dinkelberg-Hegau Region Faults
Albstadt Scherzone
Albstadt Shear Zone
According to the structure of the overburden, the southern layer plain is divided into two segments. To the west of the Lauchert-Mulde, which strikes about N-S, there is an approximately triangular block complex as a western slope of the Central Black Forest uniformly against ESE, which is bounded in the north by the Elztal and Bebenhausen fault zone, in the south by the Freiburg-Bonndorf-Lake Constance fault zone . According to the distribution of the recent earthquake epicentres, there is a left-lateral shear zone several kilometers wide in the basement, which is called the Albstadt shear zone, on the eastern edge of this western segment. The sinistral offset of this zone manifests itself on the surface in right-lateral-transtensive fractures (Hohenzollern-Graben, Achalm-Halfgraben) and in a parallel flexure-like offset of the Swabian lineament.
Nach der Struktur des Deckgebirges zerfällt das Südliche Schichtstufenland in zwei Segmente. Westlich der etwa N-S streichenden Lauchert-Mulde fällt ein im Norden von Elztal- und Bebenhausen-Störungszone, im Süden von der Freiburg–Bonn­dorf – Bodensee-Störungszone etwa dreieckig begrenzter Schollenkomplex als Westabdachung des Zentralschwarzwaldes einheitlich gegen ESE ein. Nach der Ver­teilung der rezenten Erdbeben-Epizentren befindet sich am Ostrand dieses westlichen Segments eine mehrere Kilometer breite linkslaterale Scherzone im Grundgebirge, die als Albstadt-Scherzone bezeich­net wird. Der sinistrale Versatz dieser Zone äußert sich an der Oberfläche in fiederartig ange­legten Dehnungsbrüchen (Hohenzollern-Graben, Achalm-Halbgraben) und in parallelem flexurartigem Versatz von Klifflinie und Schwäbischem Lineament.
Trochtelfinger Verwerfung 1
Trochtelfingen Fault 1
Steinhilben Fault 1
Steinhilbener Verwerfung 1
SSW-NNE striking fault, dipping ESE with unknown angle
Teck-Störung 1
Teck Fault 1
NNW-SSE streichende, nach WSW einfallende Abschiebung mit unbekanntem Einfallswinkel.
NNW-SSE striking normal fault, dipping WSW with unknown angle
N-S striking normal fault, dipping W with unknown angle
N-S streichende, nach W einfallende Abschiebung mit unbekanntem Einfallswinkel.
Trochtelfingen Fault 2
Trochtelfinger Verwerfung 2
Steinhilbe Fault 2
Steinhilbener Verwerfung 2
SSW-NNE streichende Blattverschiebung.
SSW-NNE striking strike-slip fault
Teck-Störung 3
Teck Fault 3
Teck-Störung 2
Teck Fault 2
Hohenzollern Graben is a more than 30 km long, on average 1.5 km wide graben structure of the southwestern Swabian Alb. Running in Hercynian (NW-SE) direction, it formed some 15 ma ago as a result of the tectonic tension caused by the Alpine orogeny. Its conjugate, V-shaped marginal faults feature throws of up to 100 m on the Alb Plateau, and up to 40 m in the foreland. Hohenzollern Graben manifests a conspicuous relief inversion with the trough interior jutting out its surround by up to 350 m.
Der Hohenzollern-Graben ist ein über 30 km langer und durchschnittlich 1,5 km breiter geologischer Graben im Bereich der südwestlichen Schwäbischen Alb, der sich in herzynischer Richtung (NW-SE) von der Albhochfläche bis ins Albvorland zieht. Er entstand vor ca. 15 Millionen Jahren als Folge der tektonischen Spannungen durch die Auffaltung der Alpen. Die den Hohenzollerngraben begrenzenden Randverwerfungen haben eine Sprunghöhe von rund 100 m auf der Albhochfläche und bis zu 40 m im Vorland und fallen als konjugierte Störungen V-förmig nach innen, wo sie wahrscheinlich in eine dextrale Scherzone münden, die als antithetische Nebenstörung der Nord-Süd orientierten Albstadt-Scherzone im Untergrund betrachtet wird. Der Hohenzollern-Graben zeigt eine ausgeprägte Reliefumkehr: Obwohl es sich um ein Einbruchgebiet handelt, überragt das grabeninnere Gelände seine Umgebung bis zu 350 m.
Hohenzollern-Graben
Hohenzollern Graben
Hohenzollern Graben Fault 8
Hohenzollern-Graben Störung 8
WNW-ESE streichende Blattverschiebung; Teil der Nordrandverwerfung des Hohenzollerngrabens.
WNW-ESE striking strike-slip fault; part of the northern boundary of the Hohenzollerngraben.
Hohenzollern Graben Fault 7
WNW-ESE streichende Störung, Teil der Südrandverwerfung des Hohenzollerngrabens. Nordwestlicher Abschnitt als Blattverschiebung, südöstlicher Abschnitt als Abschiebung Richtung NNE mit unbekanntem Einfallswinkel ausgeprägt.
WNW-ESE striking fault with the northwestern segemt developed as strike-slip and the southeastern part as normal fault dipping NNE with unkown angle; part of the southern boundary of the Hohenzollerngraben.
Hohenzollern-Graben Störung 7
WNW-ESE streichende, nach SSW einfallende Abschiebung mit unbekanntem Einfallswinkel; Teil der Nordrandverwerfung des Hohenzollerngrabens.
Hohenzollern Graben Fault 10
Hohenzollern-Graben Störung 10
WNW-ESE striking normal fault, dipping SSW with unknown angle; part of the northern boundary of the Hohenzollerngraben.
Hohenzollern Graben Fault 9
Hohenzollern-Graben Störung 9
WNW-ESE streichende Blattverschiebung; Teil der Südrandverwerfung des Hohenzollerngrabens.
WNW-ESE striking strike-slip fault; part of the southern boundary of the Hohenzollerngraben.
NW-SE striking normal fault, dipping NE with unknown angle, at intersection with DE-BW_227 partly strike-slip; part of the southern boundary of the Hohenzollerngraben.
NW-SE streichende, nach NE einfallende Abschiebung mit unbekanntem Einfallswinkel; an der Verschneidung mit DE-BW_227 mit Blattverschiebungskomponente; Teil der Südrandverwerfung des Hohenzollerngrabens.
Hohenzollern-Graben Störung 1
Hohenzollern Graben Fault 1
Hohenzollern Graben Fault 11
SSW-NNE striking strike-slip fault; lateral fault of the Hohenzollerngraben.
SSW-NNE streichende Blattverschiebung; Nebenstörung des Hohenzollerngrabens.
Hohenzollern-Graben Störung 11
NW-SE striking strike-slip fault; part of the northern boundary of the Hohenzollerngraben.
Hohenzollern-Graben Störung 2
Hohenzollern Graben Fault 2
NW-SE streichende Blattverschiebung; Teil der Nordrandverwerfung des Hohenzollerngrabens.
NW-SE streichende, nach SW einfallende Abschiebung mit unbekanntem Einfallswinkel; Teil der Nordrandverwerfung des Hohenzollerngrabens.
Hohenzollern-Graben Störung 4
Hohenzollern Graben Fault 4
NW-SE striking normal fault, dipping SW with unknown angle; part of the northern boundary of the Hohenzollerngraben.
Hohenzollern-Graben Störung 3
Hohenzollern Graben Fault 3
Hohenzollern Graben Fault 6
WNW-ESE striking fault with the northern segment developed as normal fault dipping SSW with unknown angle and the southern part as strike-slip; part of the northern boundary of the Hohenzollerngraben.
WNW-ESE streichende Störung; nördlicher Abschnitt als Abschiebung Richtung SSW mit unbekanntem Einfallswinkel, südlicher Abschnitt als Blattverschiebung ausgeprägt; Teil der Nordrandverwerfung des Hohenzollerngrabens.
Hohenzollern-Graben Störung 6
NW-SE streichende Blattverschiebung; an der Verschneidung mit DE-BW_223 mit Abschiebungskomponente; Teil der Südrandverwerfung des Hohenzollerngrabens.
Hohenzollern-Graben Störung 5
NW-SE striking strike-slip fault, at intersection with DE-BW_223 partly normal faulting; part of the southern boundary of the Hohenzollerngraben.
Hohenzollern Graben Fault 5
Teck-Störung 4
Teck Fault 4
N–S streichendes Abschiebungs system mit 2 Hauptstörungen
N-S striking normal fault system with two main faults
Gauinger Verwerfung
Gauingen Fault
Pfronstetten-Kettenacker-Ittenhausen Fault
Pfronstetten-Kettenacker-Ittenhausen Verwerfung
Teck-Störung 6
Teck Fault 6
SW-NE striking normal fault, downthrow of SE-block about 70 m
Lautertal Fault
Lautertal Störung
SW-NE streichende Störung, SE-Scholle etwa 70 m abgesunken
WSW-ENE streichende, nach WNW einfallende Abschiebung mit unbekanntem Einfallswinkel.
Teck-Störung 5
SSW-NNE striking normal fault, dipping WNW with unknown angle
Teck Fault 5
Indelhausen-Oberwilzingen Fault
Indelhausen-Oberwilzingen-Störung
NW-SE streichender Halbgraben, welcher neben abschiebenenden teilweise auch dextral-transtensive Bewegungsindikatoren aufweist. Diese entsprechen konjugierten antithetischen Scherflächen zu den sinistralen Gleitbewegungen des tieferen Gebirges im Bereich der Albstadt-Scherzone; nördliche Begrenzung durch Störung, Südgrenze als Flexur.
NW-SE striking single halfgraben, which shows characteristics of normal faulting and right-lateral-transtensive movement. The latter correspont to conjugated antithetical shear surfaces to the left-lateral sliding movement of the basement in the area of the Albstadt Shear Zone; northern boundary as fault, southern boundary as a flexure.
Achalm-Halfgraben
Achalm-Halbgraben
Römerstein Verwerfung
Römerstein Fault
Zwiefaltener Bruchfeld
Zwiefalten Faultzone
N-S streichende, nach E einfallende Abschiebung mit unbekanntem Einfallswinkel.
N-S striking normal fault, dipping E with unknown angle
Schlossberg Fault
Schloßberg Störung
SW-NE striking, vertical to steeply NW dipping normal fault running W to NW of Kallmünz across the Vils river valley.
SW-NE streichende, saigere bis steil nach NW einfallende Abschiebung W bis NW von Kallmünz, quer durch das Vilstal.
Ursheim Fault
Ursheim Störung
W-E striking normal fault crossing Rohrach river valley south of Schmidsberg-Hahnenberg Fault [N_11].
Das Rohrachtal querende, W-E streichende Abschiebung südlich der Schmidsberg-Hahnenberg Störung [N_11].
Sandbreite Fault
Sandbreite Störung
N-S striking, vertical to steeply E dipping normal fault with a minor throw.
N-S streichende, saigere bis steil nach E einfallende Abschiebung mit geringer Sprunghöhe.
Krachenhausen-Holzheim Fault
Krachenhausen-Holzheim Störung
W-E striking fault along Holzheimer valley.
W-E streichende Störung entlang des Holzheimer Tals.
Schwäbisch (SW-NE) streichendes Grabenbruchfeld mit Verwerfungen um 25 m, welches die Krusteneinwölbung (um 100 m auf 10 km Breite) des oberen Filstals überprägt.
Swabian (SW-NE) striking rift valley with faults of 25 m offset, overprinting the crustal vaulting (100 m over 10 km width) of the upper Fils valley.
Filstal-Graben
Filstal Graben
SSW-NNE streichende, nach WNW einfallende Abschiebung mit unbekanntem Einfallswinkel.
Filstal Graben Fault 1
Filstal-Graben Störung 1
SW-NE streichende, nach SE einfallende Abschiebung mit unbekanntem Einfallswinkel.
Mähdlesbühl-Verwerfung
SW-NE striking normal fault, dipping SE with unkown angle
Mähdlesbühl Fault
Filstal-Graben Störung 2
Filstal Graben Fault 2
Krachenhausen-Dornau Fault
Krachenhausen-Dornau Störung
NW-SE striking, steeply NE dipping normal fault.
NW-SE streichende, steil nach NE einfallende Abschiebung.
[geola_008]
SW-NE streichende, steil nach NE einfallende Abschiebung mit einer Sprunghöhe um 10 m.
Arberschlag-Hubhof Fault
Arberschlag-Hubhof Störung
SW-NE striking, steeply NE dipping normal fault with an approx. 10 m throw.
Sachsenhofen-Vogelhüll Fault
Sachsenhofen-Vogelhüll Störung
N-S striking, vertical to steeply E dipping normal fault featuring a throw of up to 15 m.
N-S streichende, saigere bis steil nach E einfallende Abschiebung mit einer Sprunghöhe bis zu 15 m.
Friedinger Störung
Frieding Fault
Mindelsee Fault
NW-SE streichende, ca. 80° nach SW einfallende Abschiebung mit um ca. 120 m abgesenkter SW-Scholle; Teil der Bodenseebrüche und NE-Randstörung des Hegau Grabens, damit Grenzlinie zwischen dem eigentlichen Molassebecken und seinem Beckenrand als Teil der Freiburg-Bonndorf-Bodensee Zone [DE-BW_913].
NW-SE striking, approx. 80 ° to SW dipping normal fault with SW downthrow block lowered by approx. 120 m. Part of the Lake Constance fractures and northeastern marginal fault of the Hegau Graben, thus the borderline between the Molasse basin proper and its basin edge as part of the Freiburg-Bonndorf-Lake Constance Zone [DE-BW_913].
Mindelsee-Verwerfung
Duggendorf Fault
Duggendorf Störung
WNW-ESE to WSW-ENE trending, steeply SSW to SSE dipping normal fault featuring a throw of up to 40 m.
WNW-ESE bis WSW-ENE verlaufende, steil nach SSW bis SSE einfallende Abschiebung mit einer Sprunghöhe bis zu 40 m.
[geola_009]
Kühschlag-Nittendorf Fault
Kühschlag-Nittendorf Störung
Kinked S-N to SSW-NNE trending, steeply E to ESE dipping normal fault.
Geknickt S-N bis SSW-NNE verlaufende, steil nach E bis ESE einfallende Abschiebung.
Kaldorf-Tafelmühle Fault
Kaldorf-Tafelmühle Störung
SW-NE striking pair of conjugate normal faults W of Titting, a SE dipping northwestern branch and a NW dipping southeastern branch, forming a local graben structure.
SW-NE streichendes Paar konjugierter Abschiebungen W von Titting, die mit einem nach SE einfallenden Nordwest-Ast und einem nach NE einfallenden Südost-Ast eine lokale Grabenstruktur begrenzen.
Preith-Walting Lineament
Predominantly W-E trending, strikingly persistent lineament, turning to a WNW-ESE trend along Affental dry valley. Due to the intense interlock of facies in the Upper Jurassic carbonates vertical and/or lateral movements cannot be verified.
Überwiegend W-E verlaufendes und auffallend langes Lineament, das entlang des Affental auf WNW-ESE umbiegt. Vertikale und/oder laterale Versätze sind aufgrund der intensiven Faziesverzahnung im Weißen Jura nicht nachzuweisen.
Mühltal Fault
Mühltal Störung
SW-NE to SSW-NNE trending, steeply SE to ESE dipping normal fault.
SW-NE bis SSW-NNE verlaufende, steil nach SE bis ESE einfallende Abschiebung.
Lichtenberg Step Fault
Lichtenbergsprung
WNW-ESE trending, approx. 70° SSE dipping, 2- to 3-stepped step fault featuring a throw of overall up to 30 m.
Südlich von Solnhofen WNW-ESE verlaufende, ca. 70° nach SSE einfallende, 2- bis 3-stufige Bruchstaffel mit einem Verwurf von insgesamt bis zu 30 m.
Schrandelbuck-Mörnsheim Fault
Schrandelbuck-Mörnsheim Störung
WNW-ESE trending, approx. 70° SSE dipping normal fault; southern scarp of Lichtenberg Step Fault.
WNW-ESE verlaufende, ca. 70° nach SSE einfallende Abschiebung; südlicher Abbruch des Lichtenbergsprungs.
Schelmenbuck-Maxberg Fault
Schelmenbuck-Maxberg Störung
WNW-ESE trending, approx. 70° SSE dipping normal fault. Main scarp of Lichtenberg Step Fault, towards the west increasingly covered by Ries Impact ejecta masses.
WNW-ESE verlaufende, ca. 70° nach SSE einfallende Abschiebung. Nach Westen hin zunehmend von Ries-Trümmermassen verdeckter Hauptabbruch des Lichtenbergsprungs.
Rohrbach Fault
Rohrbach Störung
WSW-ENE striking, steeply NNW dipping normal fault crossing Vils river valley south of Rohrbach.
WSW-ENE streichende, steil nach NNW einfallende Abschiebung; quert das Vilstal südlich von Rohrbach.
Judenbuck-Pappenheim Fault
Judenbuck-Pappenheim Störung
Slightly undulate W-E trending, steeply N dipping normal fault with a throw of up to 40 m running sub-parallel to Heunischhof-Treuchtlingen Fault [DE-BY_1262) and Schambach Fault [DE-BY_1261] forming a local graben structure in between.
Leicht gewellt W-E verlaufende, steil nach N einfallende Abschiebung mit einem Vertikalversatz von bis zu 40 m. Bildet mit den nördlich sub-parallel verlaufenden Heunischhof-Treuchtlingen [DE-BY_1262) und Schambach [DE-BY_1261] Störungen eine lokale Grabenstruktur.
Vils Valley train of faults
Vilstal Störungszug
Running from Vilshofen (with a possible northern extension as far as Ebermanndorf) to Schmidmühlen more or less along Vils river valley, array of NNW-SSE and NNE-SSW striking fault segments, partly in two branches. This overall N-S trending train of normal faults, inferred in most sections, dips steeply to the west with a minor throw of up to 15 m.
Von Vilshofen (möglicherweise bereits von Ebermannsdorf) überwiegend entlang des Vilstales bis nach Schmidmühlen ziehende Abfolge NNW-SSE und NNE-SSW streichender Störungssegmente, abschnittsweise in zwei Ästen. Dieser insgesamt N-S verlaufende, in den meisten Abschnitten vermuteter Störungszug, besteht aus steil W fallenden Abschiebungen mit einer Sprunghöhe von höchstens 15 m.
Unterödenhart Fault
Unterödenhart Störung
Running from Reisberg to Machendorf deserted hamlet, N-S to WNW-ESE trending, steeply E to NNE dipping normal fault with a minor throw.
Vom Reisberg zur Wüstung Machendorf ziehende, N-S bis WNW-ESE verlaufende, steil nach E bis nach NNE einfallende Abschiebung mit geringer Sprunghöhe.
Hohenfels-Machtelwies Fault
Hohenfels-Machtelwies Störung
Discontinuous, undulate WSW-ESE to W-E trending, steeply ± N dipping normal fault with a minor throw up to 10 m.
Diskontinuierliche, gewellt WSW-ENE bis W-E verlaufende, steil nach ± N einfallende Abschiebung mit einer geringen Sprunghöhe von höchstens 10 m.
Oberbügl-Michelsberg Fault
Oberbügl-Michelsberg Störung
NNW-SSE striking fault of unresolved kinematic.
NNW-SSE streichende Störung unbekannter Kinematic.
Thannhausen Fault
Thannhausen Störung
W-E striking, steeply N dipping normal fault.
W-E streichende, steil nach N einfallende Abschiebung.
Schellenburg Horsts Scarps
Schellenburg Horst-Flanken
Altmühl and Anlauter valleys at their confluence with Schwarzach valley at Kinding show relief inversions underneath the Quaternary alluvium, formed by SSW-NNE trending upheavals. Inferred from borehole evidence the confining steeply dipping reverse faults feature a 30 m throw (Altmühl valley) and less than 10 m (Anlauter valley). Due to lack of evidence the continuation of the horst flanks to the south as well as to the north, crossing Schwarzach valley, is uncertain. Virtual extension of the fault’s trend to the north implies a merger into / branching off or truncation by Rumburg-Kinding Fault [DE-BY_1274] and its unexposed continuation along Schwarzwald-Bayerwald Line [DE-BY_1255]. At depth, the Altmühl valley horst flanks margin a geophysically detected Permian Rotliegend trough, implying a Variscan origin and post-Jurassic reactivation of the faults.
Die Täler von Altmühl und Anlauter zeigen an ihrer Einmündung ins Schwarzachtal bei Kinding unter der quartären Talfüllung eine Reliefumkehr, hervorgerufen durch SSW-NNE (rheinisch) streichende, Horst-artige Strukturen. Die begrenzenden, steil einfallenden Aufschiebungen weisen, abgeleitet aus Bohloch-Korrelationen, Sprunghöhen von 30 m (Altmühltal) und weniger als 10 m (Anlautertal) auf. Wegen fehlender Geländenachweise ist die Fortsetzung der Horst-Flanken nach Süden wie Norden (im und jenseits des Schwarzachtals) hin, ungeklärt. Eine virtuelle Verlängerung der Horst-Flanken nach Norden, deutet auf eine Konfluenz mit der oder Kappung durch die Rumburg-Kinding Störung [DE-BY_1274] hin, bzw. ihrer nicht aufgeschlossenen Verlängerung entlang der Schwarzwald-Bayerwald Linie [DE-BY_1255]. Die Flanken des Altmühltal Horstes begrenzen auch den geophysikalisch nachgewiesenen Rotliegend Trog in der Tiefe; eine variskische Anlage und post-jurassische Reaktivierung der Brüche ist daher anzunehmen.
Hattenhausen Fault
NW-SE streichende, steil nach SW einfallende Abschiebung.
Hattenhausen Störung
Frauenleite Fault
Frauenleite Störung
W-E trending, steeply S dipping two-step normal fault NW of Kinding.
Nordwestlich von Kinding W-E verlaufende, steil nach S einfallende zweistufige Abschiebung.
Lautersee Fault
Lautersee Störung
West of Painten NNW-SSE striking, steeply WSW dipping normal fault with a throw of about 10 m.
Westlich von Painten NNW-SSE streichende, steil nach WSW einfallende Abschiebung mit einer Sprunghöhe um 10 m.
Euerwang Fault
Euerwang Störung
South of Euerwang WNW-ESE striking, steeply S dipping normal fault featuring a throw of up to 15 m.
Südlich von Euerwang WNW-ESE streichende,steil südfallende Abschiebung mit einer Sprunghöhe von bis zu 15 m.
Western Part of the Schwarzwald-Bayerwald Line, a principal fault zone cutting WSW-ENE to W-E through southern Germany. Multi-phase oblique-slip fault system, west of the Ries Impact Crater [DE-BY_1342], in Baden-Württemberg, as the WSW-ENE striking Swabian Lineament traceable in the Upper Jurassic carbonates between Heubach W Aalen and the Ries crater only, in few predominantly steeply S dipping fault segments featuring throws from 20 to 100 m.
Westlicher Abschnitt der Schwarzwald-Bayerwald Linie, einer bedeutenden Störungszone die sich in WSW-ENE bis W-E Richtung quer durch Süddeutschland verfolgen lässt. Mehrphasiges Schrägabschiebungssystem das sich westlich des Rieskraters [DE-BY_1342], in Baden-Württemberg, als WSW-ENE streichendes Schwäbische Lineament nur abschnittsweise als überwiegend steil südfallende Störung mit Vertikalversätzen von 20 bis 100 m manifestiert und von Heubach W Aalen bis zum Ries durch die oberjurassischen Karbonate zieht. Zwischen den Schollen nördlich und südlich des Schwäbischen Lineaments besteht ein nur unbedeutender Höhenversatz, die großen Sprunghöhen liegen zwischen den Teilschollen im Inneren der Störungszone.
Swabian Lineament
Schwäbisches Lineament
Hohenstaufen Störungszone
Hohenstaufen Fault Zone
SW-NE streichendes sinistrales Störungssystem zwischen Fildergraben und Ries; vertikale Versatzbeträge wechseln innerhalb kurzer Distanzen stark. Östlicher Abschnitt des Schwäbischen Lineaments.
SW-NE striking left-lateral fault system between the Fildergaben and Ries; vertical offset vary greatly within short distances. Eastern section of the Swabian lineament.
Hohenstaufen Störungszone Fiederstruktur 1
WNW-ESE striking strike-slip fault, as horsetail splay structure part of the swabian lineament
Hohenstaufen Fault Zone - Fault 1
Teil des Schwäbischen Lineaments
Hohenstaufen Fault Zone - Fault 12
W-E streichende Blattverschiebung.
Hohenstaufen Störungszone Verwerfung 12
W-E striking strike-slip fault
Hohenstaufen Fault Zone - Fault 11
Hohenstaufen Störungszone Verwerfung 11
Hohenstaufen Störungszone Fiederstruktur 3
Hohenstaufen Fault Zone - Fault 3
WNW-ESE streichende Blattverschiebung; als Fierderstruktur Teil des Schwäbischen Lineamentes
Hohenstaufen Störungszone Fiederstruktur 2
Hohenstaufen Fault Zone - Fault 2
Hohenstaufen Fault Zone - Fault 5
Hohenstaufen Störungszone Verwerfung 5
Hohenstaufen Fault Zone - Fault 4
Hohenstaufen Störungszone Verwerfung 4
Hohenstaufen Fault Zone - Fault 7
Hohenstaufen Störungszone Verwerfung 7
Hohenstaufen Fault Zone - Fault 6
Hohenstaufen Störungszone Verwerfung 6
Hohenstaufen Fault Zone - Fault 8
Hohenstaufen Störungszone Verwerfung 8
Hohenstaufen Störungszone Verwerfung 10
Hohenstaufen Fault Zone - Fault 10
Hohenstaufen Fault Zone - Fault 9
Hohenstaufen Störungszone Verwerfung 9
Schwäbisches Lineament 2
Swabian Lineament 2
Schwäbisches Lineament 1
Swabian Lineament 1
Swabian Lineament 4
Schwäbisches Lineament 4
Schwäbisches Lineament 3
Swabian Lineament 3
Riedenburg Fault
Riedenburg Störung
SSW-NNE striking, steeply WNW dipping normal fault featuring a throw of more than 100 m.
SSW-NNE streichende, steil nach WNW einfallende Abschiebung mit einer Sprunghöhe von über 100 m.
Erlinghofen Fault
Erlinghofen Störung
North of Erlinghofen WSW-ENE striking, steeply SSE dipping two-step normal fault with a cumulative throw of about 20 m.
Nördlich von Erlinghofen WSW-ENE streichende, steil nach SSE einfallende zweistufige Abschiebung mit einer Gesamtsprunghöhe von etwa 20 m.
Maierleite-Breitenbrunn Fault
Maierleite-Breitenbrunn Störung
W-E striking, steeply S dipping normal fault featuring a throw of up to 25 m.
W-E streichende, steil nach S einfallende Abschiebung mit einem Vertikalversatz von bis zu 25 m.
Fuchsberg Störung
NNW-SSE striking, steeply ENE dipping normal fault east of Titting.
NNW-SSE streichende, steil nach ENE einfallende Abschiebung östlich von Titting.
Fuchsberg Fault
Parsberg Fault
Parsberg Störung
SSW-NNE striking, steeply ESE dipping normal fault featuring a throw up to 25 m.
SSW-NNE streichende, steil nach ESE einfallende Abschiebung mit einer Sprunghöhe bis zu 25 m.
Grünschlag-Neuhof Fault
Grünschlag-Neuhof Störung
NW-SE to NNW-SSE trending, vertical to steeply NE to ENE dipping normal fault featuring a throw of up to 30 m.
NW-SE bis NNW-SSE verlaufende, vertikale bis steil nach NE bis ENE einfallende Abschiebung mit einer Sprunghöhe bis 30 m.
Mitterbügl Cross Fault
Mitterbügl Querstörung
SW-NE trending oblique-slip fault with a small-scale dextral movement, displacing Grünschlag-Neuhof Fault, and a minor vertical movement of less than 10 m.
SW-NE verlaufende Schrägabschiebung mit einer kleinräumigen dextralen Bewegungsrichtung, die die Grünschlag-Neuhof Störung versetzt, und einem Vertikalversatz von weniger als 10 m.
Ammerfeld-Rohrbach Fault
Ammerfeld-Rohrbach Störung
NW-SE trending, steeply NE dipping normal fault, southwestern flank of Asbrunner Graben (Streit 1978).
NW-SE streichende, steil nach NE einfallende Abschiebung; südwestliche Begrenzung des Asbrunner Grabens (Streit 1978).
Eibichel-Treidelheim Fault
Eibichel-Treidelheim Störung
NNW-SSE to NW-SE trending, steeply WSW to SW dipping normal fault; in its western section forming the northeastern flank of Asbrunner Graben (Zeiss 1964, Streit 1978).
NNW-SSE bis NW-SE verlaufende, steil nach WSW bis SW einfallende Abschiebung; bildet im westlichen Abschnitt die nordöstliche Begrenzung des Asbrunner Grabens (Zeiss 1964, Streit 1978).
Crossing the Wellheim dry valley NW of Konstein, SW-NE striking, approx. 70° NW dipping normal fault featuring a throw up to 60 m.
Konstein Fault
Konstein Störung
Das Wellheimer Trockental NW von Konstein kreuzende, SW-NE streichende, ca. 70° nach NW fallende Abschiebung mit einer Sprunghöhe bis zu 60 m.
Spindeltal-Gammersfeld Fault
Gammersfelder Sprung
Gammersfeld-Eulahof Verwerfung
Spindeltal-Gammersfeld Störung
NNW-SSE trending, steeply (85°-60°) WSW dipping normal fault featuring a throw up to 40 m.
NNW-SSE verlaufende, steil (85°-60°) nach WSW einfallende Abschiebung mit einer Sprunghöhe bis zu 40 m.
Hagenau Fault
Hagenausprung
Predominantly WSW-ENE trending, at its western limb veering to NNW-SSE, steeply (85°-60°) SSE to WSW dipping normal fault featuring a throw of about 10 m, distributed among two fault scarps in the east.
Überwiegend WSW-ENE verlaufende, an ihrem westlichen Ende auf NNW-SSE abbiegende, steil (85°-60°) nach SSE bis WSW einfallende Abschiebung mit einem Verwurf von insgesamt rund 10 m, im Osten aufgeteilt auf zwei Bruchstaffeln.
Schafshill-Neuenhizenhausen Fault
Schafshill-Neuenhizenhausen Störung
N-S striking, steeply W dipping normal fault featuring a throw of about 50 m.
N-S streichende, steil nach W einfallende Abschiebung mit einer Sprunghöhe um 50 m.
Principal fault zone cutting WSW-ENE to W-E through southern Germany. Multi-phase oblique-slip fault system, in Bavaria traceable only in few predominantly steeply S dipping fault segments in Upper Jurassic subcrops, featuring a throw rarely exceeding 50 m, or as flexures. The main phase of deformation, mainly a dextral movement with a significant vertical component resulting in throws up to 300 m, is assigned to Late Variscan, as inferred from seismic evidence at the edge of Permo-Carboniferous troughs at depth.
Bedeutende Störungszone die sich in WSW-ENE bis W-E Richtung quer durch Süddeutschland verfolgen lässt. Mehrphasiges Schrägabschiebungssystem das in Bayern nur abschnittsweise als überwiegend steil südfallende Störung der jurassischen Oberfläche mit Versätzen von selten über 50 m oder als Flexur nachweisbar ist. Die am Rand permokarbonischer Tröge in der Tiefe geophysikalisch ermittelten Versätze bis zu 300 m implizieren, dass die spätvariszische Hauptbewegungsphase mit überwiegend dextral seitenverschiebendem Bewegungssinn auch eine deutliche Vertikalkomponente umfasste.
Schwarzwald-Bayerwald Line
Schwäbisch-Fränkisches Lineament
Schwarzwald-Bayerwald-Linie
Kareth Step Fault
Karether Störungszone
Kareth Bruchstaffel
W-E to WNW-ESE trending steeply (85°-60°) S to SSW dipping step fault crossing the Regen river valley immediately north of its junction with Danube river valley. This 3-stepped fault featuring a cumulative throw of less than 20 m is deemed the northernmost branch of the forking western continuation of the Donaurand Fault Scarp [DE-BY_698] (Bauberger et al. 1969).
W-E bis WNW-ESE verlaufende, steil (85°-60°) nach S bis SSW einfallender Staffelbruch der das Regental unmittelbar nördlich der Regen Mündung in die Donau quert. 3-stufiger Abbruch mit einer Gesamtsprunghöhe von unter 20 m, der als nördlichster Zweig der sich verzweigenden Fortsetzung des Donaurandbruchs [DE-BY_698] angesehen wird (Bauberger et al. 1969).
Kneiting-Pfaffenstein Fault
Kneiting-Pfaffenstein Störung
W-E trending, steeply (85°-60°) S dipping normal fault subcropping between Kneiting and mouth of Regen river. Subordinate (northern) branch of western continuation of Donaurand Fault Scarp [DE-BY_698], assigned to Schwarzwald-Bayerwald-Line.
W-E verlaufende, steil (85°-60°) nach S einfallende Abschiebung zwischen Kneiting und der Regen Mündung. Subordinate (nördlicher) Zweig der westlichen Fortsetzung des Donaurandbruchs [DE-BY_698], die der Schwarzwald-Bayerwald-Linie zugerechnet wird.
Deuerling Fault
Deuerlinger Störung
Deuerling Störung
W-E trending, approx. 70° S dipping normal fault with a throw up to 80 m. Subcropping between Hohenschambach and Tegernheim in parts as a step fault in two subparallel branches. Main (southern) branch of western continuation of Donaurand Fault Scarp [DE-BY_698]. Assigned to Schwarzwald-Bayerwald-Line and part of Regensburg Confluence in the sense of Schwarz (2012).
W-E verlaufende, ca. 70° nach S einfallende Abschiebung, streckenweise als zweistufiger Staffelbruch, mit einer kumulativen Sprunghöhe bis zu 80 m. Nur teilweise aufgeschlossene Störung zwischen Hohenschambach und Tegernheim als Hauptast der westlichen Fortsetzung des Donaurandbruchs [DE-BY_698]. Teil der Regensburger Konfluenz im Sinne von Schwarz (2012), die der Schwarzwald-Bayerwald Linie zugeschrieben wird.
Wachenzell-Altdorf Lineament
Altdorfer Flexur
This striking lineament along "Blaubrunnental" dry valley implies that at least certain segments of the "Altdorfer Flexur" (Freyberg 1969), as inferred from narrowing intervals of Upper Jurassic contour lines, have been deformed by brittle tectonics.
Das auffällige Lineament entlang des Blaubrunnentals impliziert, dass zumindest einige Abschnitte der "Altdorfer Flexur" (Freyberg 1969), abgeleitet aus dem Zusammenrücken der Streichlinien, einer bruchhaften Verformung unterlagen.
Rumburg-Kinding Fault
Rumburg-Kinding Störung
SW-NE trending, steeply SE dipping normal fault with a minor throw passing into a WSW-ENE trending flexure to the west ("Altdorfer Flexur" [DE-BY_1275]).
SW-NE verlaufende, steil nach SE einfallende Abschiebung mit geringer Sprunghöhe, die nach Westen hin in eine WSW-ENE verlaufende Flexur übergeht ("Altdorfer Flexur" [DE-BY_1275]).
Töging Fault
Töging Störung
Running southerly parallel to Ottmaring Fault [DE-BY_1270], W-E striking, steeply S dipping normal fault featuring a throw of up to 20 m. Assumedly a section of a suppositious southern offset of Schwarzwald-Bayerwald Line [DE-BY_1255] continuing in Mühlbach Fault [DE-BY_1271] and Kumpfhof Fault [DE-BY_1269] to the east.
Südlich parallel zur Ottmaring Störung [DE-BY_1270] verlaufende, W-E streichende, steil nach S einfallende Abschiebung mit einer Sprunghöhe bis zu 20 m. Vermutlich Teil des hypothetischen Süd-Astes der Schwarzwald-Bayerwald Linie [DE-BY_1255] der sich nach Osten hin in den Mühlbach [DE-BY_1271] and Kumpfhof [DE-BY_1269]] Störungen fortsetzt.
Schmidsberg-Hahnenberg Fault
Schmidsberg-Hahnenberg Störung
Crossing Rohrach river valley, W-E trending, steeply S dipping normal fault emerging from the Ries Impact ejecta masses in the west.
Das Rohrachtal querende, W-E verlaufende, steil nach S einfallende Abschiebung, die sich östlich der Ries-Trümmermassen verfolgen lässt.
Schlossberg Subfault
Schloßberg Nebenstörung
W-E striking branch of Schmidsberg-Hahnenberg Fault running parallel north of the main fault.
W-E streichende nördlich parallel zur Schmidsberg-Hahnenberg Störung verlaufender Seitenast.
Stahlmühle Subfault
Stahlmühle Zweigstörung
WSW-ENE striking side branch of Schmidsberg-Hahnenberg Fault.
WSW-ENE streichender Seitenast der Schmidsberg-Hahnenberg Störung.
Nur selten zu Tage tretender Abschnitt der Schwarzwald-Bayerwald-Linie zwischen Beilngries und östlich von Dietfurt. WNW-ESE verlaufende, ± saigere bis steil SSE oder NNW einfallende Abschiebung mit einer Sprunghöhe von etwa 40 m.
Beilngries-Dietfurt Fault
Beilngrieser Verwerfung
Beilngries-Dietfurt Störung
Largely subcropping segment of Schwarzwald-Bayerwald-Line running from Beilngries to the east of Dietfurt. WNW-ESE trending ± vertical to steeply SSE or NNW dipping normal fault featuring a throw of about 40 m.
Hellafelsen Querstörung
SW-NE striking, steeply NW dipping link of Ottmaring Fault [DE-BY_1270] and Beilngries-Dietfurt Fault [DE-BY_1259].
SW-NE streichende, steil nach NW einfallende Verbindung von Ottmaring [DE-BY_1270] und Beilngries-Dietfurt [DE-BY_1259] Störung.
Mühlbach Störung
NW-SE striking, turning to a W-E strike, steeply NE to N dipping normal fault with a throw of up to 30 m. The fault's southern, W-E striking part assumedly is a section of the suppositious southern offset of Schwarzwald-Bayerwald Line [DE-BY_1255] continuing in Kumpfhof Fault [DE-BY_1269] to the east and Töging Fault [DE-BY_1273] to the west.
NW-SE streichende, im Süden nach W-E umbiegende, steil nach NE bis N einfallende Abschiebung mit einer Sprunghöhe von bis zu 30 m. Der südliche, W-E streichende Abschnitt der Störung ist vermutlich Teil des hypothetischen Süd-Astes der Schwarzwald-Bayerwald Linie [DE-BY_1255] der sich nach Osten hin in der Kumpfhof Störung [DE-BY_1269], nach Westen hin in der Töging Störung [DE-BY_1273] Störungen fortsetzt.
Ottmaring Fault
Ottmaring Störung
Southerly subparallel to Beilngries-Dietfurt Fault [DE-BY_1259] WNW-ESE trending, steeply SSE dipping normal fault featuring a throw of less than 20 m.
Südlich subparallel zur Beilngries-Dietfurt Störung [DE-BY_1259] WNW-ESE verlaufende, steil nach SSE einfallende Abschiebung mit einem Vertikalversatz von höchstens 20 m.
Kumpfhof Fault
Kumpfhof Störung
W-E trending, steeply N dipping normal fault with a throw of up to 25 m, running southerly parallel to the inferred trend of Schwarzwald-Bayerwald Line [DE-BY_1255]. Assumedly part of a hypothetic southern offset of that suture continuing in Mühlbach Fault [DE-BY_1271] and Töging Fault [DE-BY_1273] to the west.
W-E verlaufende, steil nach N einfallende Abschiebung mit einer Sprunghöhe bis zu 25 m, südlich parallel zum vermuteten Verlauf der Schwarzwald-Bayerwald Line [DE-BY_1255] als mutmaßlicher Abschnitt eines hypothetischen südlichen Seitenasts dieser Sutur, der auch die Mühlbach Störung Fault [DE-BY_1271] und Töging Störung [DE-BY_1273] im Westen umfasst.
Heumödern-Treuchtlingen Fault
Heumödern-Treuchtlingen Störung
WSW-ENE to W-E striking, approx. 70° ± S dipping normal fault featuring an approx. 100 m throw in the west and 30 m in the east. Assigned to Schwarzwald-Bayerwald-Line; main-branch of the Treuchtlingen Confluence in the sense of Schwarz (2012), continuing in Schambach Fault [DE-BY_1261] to the east.
Von WSW-ENE auf W-E Streichen abknickende, ca. 70° nach ± S einfallende Abschiebung mit einer Sprunghöhe von etwa 100 m im Westen und ca. 30 m im Osten, die der Schwarzwald-Bayerwald Linie zugerechnet wird. Hauptast der Treuchtlinger Konfluenz im Sinne von Schwarz (2012). Setzt sich jenseits der Treuchtlinger Talspinne in der Schambach Störung [DE-BY_1261] fort.
Heumödern-Dietfurt Fault
Heumödern-Dietfurt Störung
Undulate, NW-SE to WNW-ESE trending normal fault branching off Heumödern-Treuchtlingen Fault to the southeast and in following Heumödern valley in large parts. Side-branch of the Treuchtlingen Confluence in the sense of Schwarz (2012).
Gewellt NW-SE bis WNW-ESE verlaufende Abschiebung mit einer Sprunghöhe bis über 60 m. Von der Heumödern-Treuchtlingen Störung nach SE abzweigender, dem Heumöderntal folgender Nebenast der Treuchtlinger Konfluenz im Sinne von Schwarz (2012).
Treuchtlingen Subfault
Treuchtlingen Zweigstörung
NW-SE trending, steeply SW dipping normal fault featuring a throw up to 20 m, southeastwardly branching off Heumödern-Treuchtlingen Fault [DE-BY_1262]. Side-branch of the Treuchtlingen Confluence in the sense of Schwarz (2012).
NW-SE verlaufende, steil nach SW einfallende Abschiebung mit einer Sprunghöhe von bis zu 20 m. Von der Heumödern-Treuchtlingen Störung [DE-BY_1262] südostwärts abzweigender Nebenast der Treuchtlinger Konfluenz im Sinne von Schwarz (2012).
Schambach Fault
Schambach Störung
Undulate, overall W-E striking, approx. 70° S dipping normal fault featuring an approx. 30 m throw, assigned to Schwarzwald-Bayerwald-Line. Eastern continuation of Heumödern-Treuchtlingen Fault [DE-BY_1262].
Gewellt, insgesamt W-E streichende, ca. 70° nach S einfallende Abschiebung mit einer Sprunghöhe von etwa 30 m die der Schwarzwald-Bayerwald Linie zugerechnet wird. Östliche Fortsetzung der Heumödern-Treuchtlingen Störung [DE-BY_1262].
Lohrmannshof Fault
Lohrmannshof Störung
Largely subcropping, W-E trending fault assigned to Schwarzwald-Bayerwald Line. Inferred from westward adjoining segments, Schmidt-Kaler (1990) assumes an approx. 70° S dipping normal fault with a throw of about 30 m, passing over into a flexure to the east (Schwarz 2012, "Altdorfer Flexur" after Freyberg 1969).
W-E verlaufende, nur selten aufgeschlossene Störungslinie die der Schwarzwald-Bayerwald Linie zugerechnet wird. Aus den Verhältnissen in westlich benachbarten Abschnitten wird eine 70° nach S einfallende Abschiebung mit einer Sprunghöhe um 30 m angenommen (Schmidt-Kaler 1990), die nach Osten hin in eine Flexur übergeht (Schwarz 2012, "Altdorfer Flexur" nach Freyberg 1969).
Lohrmannshof Subfault
Lohrmannshof Zweigstörung
NW-SE striking side branch of Lohrmannshof Fault, formed by a steeply SW dipping normal fault.
NW-SE streichender Abzweig der Lohrmannshof Störung, der eine steil nach SW einfallende Abschiebung bildet.
Antoniholz Cross Fault
Antoniholz Querstörung
NW-SE trending, steeply SW dipping normal fault crossing Wachenzell-Altdorf Lineament with a NE dipping side branch branching off SE of that lineament.
Das Wachenzell-Altdorf Lineament kreuzende, NW-SE verlaufende, steil nach SW einfallende Abschiebung mit einem NE fallenden Seitenast südwestlich des Lineaments.
Mödingen Fault
Mödinger Abbruch
Emerging from Riedheim-Wittislingen Fault [DE-BY_1250], SW-NE trending, steeply (85°-60°) SE dipping normal fault featuring a throw of approx. 50 m.
Fortsetzung der Riedheim-Wittislingen Störung [DE-BY_1250], SW-NW streichende, steil (85°-60°) nach SE einfallende Abschiebung mit einer Sprunghöhe von ca. 50 m.
Lenting-Hepberg Fault
Lenting-Hepberg Störung
Conjugate pair of SSW-NNE striking normal faults, an ESE dipping western branch and a WNW dipping eastern branch, both featuring a throw of up to 12 m, thereby forming a local graben structure truncated by Hepberg Cross Fault [DE-BY_ DE-BY_1304] in the north.
Konjugiertes Paar SSW-NNE streichender Abschiebungen, die mit einem nach ESE einfallenden West-Ast und einem nach WNE einfallenden Ost-Ast, bei einem vertikalen Versatz von bis zu 12 m, eine lokale, von der Hepberg Querstörung [DE-BY_DE-BY_1304] im Norden abgeschnittene Grabenstruktur begrenzen.
Bittenbrunn-Sehensand Fault
Bittenbrunn-Sehensand Störung
Eastward arcuate overall N-S trending, steeply W dipping normal fault transecting the Neuburg Jurassic Spur across the Danube river valley.
Ostwärts gebogen, insgesamt N-S verlaufende, steil nach W einfallende Abschiebung, die den Neuburger Jurasporn über das Donautal hinweg durchschneidet.
Pfaffengrund Fault
Pfaffengrunder Querbruch
W-E trending, steeply S dipping normal fault, probably displacing the southern continuation of the Bergen Fault [DE-BY_1300] as Bittenbrunn-Sehensand Fault [DE-BY_1302] to the west.
W-E verlaufende, steil nach S einfallende Abschiebung, die wahrscheinlich die südliche Fortsetzung der Bergener Verwerfung [DE-BY_1300] als Bittenbrunn-Sehensand Störung [DE-BY_1302] nach Westen hin versetzt.
Bergen Fault
Bergener Verwerfung
NW-SE to NNW-SSE trending, steeply SW to WSW dipping normal fault, possibly continuing in the Bittenbrunn-Sehensand Fault [DE-BY_1302] displaced to the west by the Pfaffengrund Fault [DE-BY_1301].
NW-SE bis NNW-SSE verlaufende, steil nach SW bis WSW einfallende Abschiebung, die sich nach Süden hin, durch den Pfaffengrunder Querbruch [DE-BY_1301] nach Westen versetzt, möglicherweise in der Bittenbrunn-Sehensand Fault [DE-BY_1302] fortsetzt.
Arcuate NW-SE to WNW-ESE trending, steeply SW dipping normal fault featuring a throw of up to 50 m.
Hainberg-Gietlhausen Fault
Hainberg-Gietlhausen Störung
Gebogen NW-SE bis WNW-ESE verlaufende, steil nach SW einfallende Abschiebung mit einer Sprunghöhe von bis zu 50 m.
Slightly undulate NW-SE trending, steeply SW dipping normal fault featuring a throw of up to 80 m.
Frauenholz-Hainberg Fault
Frauenholz-Hainberg Störung
Leicht gewellt NW-SE verlaufende, steil nach SW einfallende Abschiebung mit einer Sprunghöhe bis zu 80 m.
Theissing-Dünzing Fault
Theißing-Dünzinger Störung
Theißing-Dünzing Störung
NNW-SSE striking, WSW dipping normal fault with a throw of up to 40 m, inferred from Upper Jurassic contour line pattern.
NNW-SSE streichende, nach WSW einfallende Abschiebung mit einer Sprunghöhe bis zu 40 m, abgeleitet aus dem Streichlinienmuster im Malm.
Demling-Vohburg Fault
Demling-Vohburg Störung
NNW-SSE striking, WSW dipping normal fault subcropping between Demling and Auhöfe; its continuation as a blind fault underneath the Molasse sediments to S of Vohburg is assumed.
NNW-SSE streichende, nach WSW einfallende Abschiebung, die Zwischen Demling und Auhöfe nur selten aufgeschlossen ist und sich unter Molasse-Überdeckung wahrscheinlich bis S Vohburg fortsetzt.
Kösching-Bettbrunn Fault
Kösching-Bettbrunner Störung
Kösching-Bettbrunn Störung
SSW-NNE striking, steeply WNW dipping normal fault featuring a throw of more than 30 m in its middle segment.
SSW-NNE streichende, steil nach WNW einfallende Abschiebung mit einer Sprunghöhe bis über 30 m im mittleren Abschnitt.
Hepberg Cross Fault
Hepberg Querstörung
W-E striking, steeply N dipping normal fault with a throw up to 15 m and truncating the western branch of Lenting-Hepberg Fault [DE-BY_ DE-BY_1303].
W-E streichende, steil nach N einfallende Abschiebung mit einer Sprunghöhe bis zu 15 m. Nördliche Begrenzung der von der Lenting-Hepberg Störung [DE-BY_DE-BY_1303] gebildeten Grabenstruktur.
Ries Crater Rim
Ries Kraterrand
Struktureller Kraterrand
This most striking structural feature of the Swabian-Franconian Alb, overlapping its northern escarpment at the border of Baden-Württemberg and Bavaria, is atectonic: the almost circular outer rim of the Ries crater formed by an asteroid impact about 14.6 million years ago in the Miocene, leaving a rampart crater of 24 km in diameter. The Ries outer rim is formed by a concentric array of blind listric faults (concave curved normal faults) resulting from slumping of mega-blocks when the over-steep impact crater flanks collapsed.
Die auffälligste Struktur der Schwäbisch-Fränkischen Alb, die im Grenzgebiet zwischen Schwäbischer und Fränkischer Alb den Albtrauf großflächig überdeckt, ist atektonisch: der annähernd kreisrunde Kraterrand des Ries Asteroiden-Einschlagskraters, entstanden vor rund 14,6 Millionen Jahren im Miozän mit einem Durchmesser von rund 24 km. Der Ries Kraterrand wird von überdeckten, konzentrischen listrischen (konkav gebogenen) Abschiebungen aufgebaut, die durch Groß-Rutschungen (parautochthone Schollen) beim Kollaps der übersteilten Einschlagskraterwände entstanden.
Egertallinie 1
Eger Valley Line 1
[geola_002]
Egertallinie 3
Eger Valley Line 3
Egertallinie 2
Eger Valley Line 2
Ipf North-South Fault
Ipf-Nord-Süd-Sprung
Nebenstörung Ipf-Nord-Süd-Sprung
Ipf North-South Subfault
Viehhausen-Bergmatting Fault
Viehausener Verwerfung
Viehhausen-Bergmatting Störung
NW-SE striking, ± vertical normal fault with a throw up to 10 m.
NW-SE streichende, ± vertikale Abschiebung mit einer Sprunghöhe von bis zu 10 m.
Bergmatting-Lohstadt Fault
Bergmatting-Lohstadt Störung
N-S striking branch of Viehhausen-Bergmatting Fault. Vertical to steepy E dipping normal fault feauring a throw up to more than 20 m.
N-S streichender Zweig der Viehhausen-Bergmatting Störung. Saigere bis steil ostfallende Abschiebung mit einem Vertikalversatz bis über 20 m.
Saxberg-Lohstadt Fault
Saxberg-Lohstadt Störung
Southwestward arcuate, NNW-SSE to WNW-ESE trending along Kunzwies Valley, vertical to steeply ± SW dipping normal fault with a 20 m throw.
Südwestwärts gebogen NNW-SSE bis WNW-ESE entlang des Kunzwiestals verlaufende, vertikal bis steil südfallende Abschiebung mit einem Vertikalversatz von bis zu 20 m.
Palmberg-Dachsberg Fault
Palmberger Verwerfung
Dachsberg-Verwerfung
Palmberg-Dachsberg Störung
Undulate, overall W-E trending, in sections branching out into small-scale faults and/or displaced by lateral faults, vertical to steepy S to SW dipping normal fault running from NE of Essing to NW of Kapfelberg. In the west, "Palmberg Fault" features a throw of up to 40 m, in its eastern leg (Dachsberg Fault), up to 60 m.
Von Riedhof NE Essing bis zum Dachsberg NW Kapfelberg gewellt, insgesamt W-E verlaufende Störung, abschnittweise zu Kleinststörungen aufgefiedert und/oder durch Querstörungen versetzt. Vertikale bis steil süd- bis südwestfallende Abschiebung mit Sprunghöhen im Westen von bis 40 m (Palmberger Verwerfung), im Osten bis 60 m (Dachsberg-Verwerfung).
Weltenburg-Mitterfecking Fault Swarm
Weltenburg-Mitterfecking Störungsschar
Array of WNW-ESE to NW-SE trending small-scale normal faults south to southeast of Kelheim, possibly portions of a branching on-strike continuation of blind Schierling Fault [DE-BY_752].
Abfolge WNW-ESE bis NW-SE verlaufender Kleinabschiebungen südlich bis südöstlich von Kelheim. Möglicherweise Segmente einer aufgefiederten Fortsetzung im Streichen der überdeckten Schierling Störung [DE-BY_752].
Schwabner Berg Fault
Schwabner Berg Störung
Slightly kinked WNW-ESE trending, steeply (85°-60°) SSW dipping normal fault with a throw up to 20 m, across the Danube River north of Hienheim.
Leicht geknickt WNW-ESE verlaufende, steil (85°-60°) nach SSW einfallende Abschiebung mit einer Sprunghöhe von bis zu 20 m; quert das Donautal nördlich von Hienheim.
Abusina-Sandharlanden Fault
Abusina-Sandharlanden Störung
WNW-ESE striking, steeply (85°-60°) SSW dipping normal fault with a throw up to 20 m running from the Roman fort ruins of Abusina S of Eining to Sandharlanden. The (subthermal) water supply of the Roman thermae at Abusina seems to be a manifestation of this fault. The on-strike continuation across the Danube River is inferred from the straight-lined dry valley Hochtal west of the Danube.
WNW-ESE streichende, steil (85°-60°) nach SSW einfallende Abschiebung mit einer Sprunghöhe von bis zu 20 m zwischen dem Römerkastell Abusina S von Eining und Sandharlanden. Die subthermale Wasserversorgung der römischen Therme Abusina steht wahrscheinlich im Zusammenhang mit dieser Störung, deren westliche Verlängerung aus dem im Streichen geradlinigen Verlauf eines Trockentals jenseits der Donau abgeleitet wurde.
The Lauchert Graben, between Veringenstadt and the ruins of Hertenstein, clearly recognizable as a morphological deepening, is a Rhenish striking (N-S), Miocene-Pliocene tectonic graben about eleven kilometers long, with a maximum throw of the visible trench shoulder of 100 m today. Its continuation to the south and north is morphologically not recognizable but evideced by seismic surveys.
Der Lauchertgraben ist ein zwischen Veringenstadt und der Ruine Hertenstein als morphologische Eintiefung deutlich erkennbarer, rund elf Kilometer langer rheinisch (N-S) streichender, miozän-pliozäner tektonischer Graben, mit einer maximalen Sprunghöhe der sichtbaren Grabenschulter von heute 100 m. Seine Fortsetzung nach Süden und Norden ist morphologisch nicht erkennbar, aber durch seismische Messungen nachgewiesen.
Lauchertgraben
Lauchert Graben
N-S streichende, nach W einfallende Abschiebung mit unbekanntem Einfallswinkel; Südicher Abschnitt der Östlichen Randstörung des Lauchertgrabens
N-S striking normal fault, dipping W with unknown angle; southern part of the eastern boundary of the Lauchertgraben.
Lauchertgraben Fault 2
Lauchertgraben Störung 2
N-S striking normal fault, dipping E with unknown angle; western boundary of the Lauchertgraben.
Lauchertgraben Fault 1
N-S streichende, nach E einfallende Abschiebung mit unbekanntem Einfallswinkel, westliche Randstörung des Lauchertgrabens.
Lauchertgraben Störung 1
SSW-NNE striking normal fault, dipping WNW with unknown angle; northern part of the the eastern boundary of the Lauchertgraben.
Lauchertgraben Fault 4
SSW-NNE streichende, nach WNW einfallende Abschiebung mit unbekanntem Einfallswinkel; nördlicher Abschnitt der östlichen Randstörung des Lauchertgrabens.
Lauchertgraben Störung 4
SSW-NNE streichende, nach WNW einfallende Abschiebung mit unbekanntem Einfallswinkel; östliche Randstörung des Lauchertgrabens.
Lauchertgraben Fault 3
SSW-NNE striking normal fault, dipping WNW with unknown angle; eastern boundary of the Lauchertgraben.
Lauchertgraben Störung 3
Lauchertgraben Störung 5
Lauchertgraben Fault 5
WNW-ESE streichende, nach SSW einfallende Abschiebung mit unbekanntem Einfallswinkel; nördliche Querstörung Lauchertgraben.
WNW-ESE striking normal fault, dipping SSW with unknown angle; northern lateral fault of the Lauchertgraben.
WNW-ESE streichende, nach SSW einfallende Abschiebung mit unbekanntem Einfallswinkel; südliche Querstörung Lauchertgraben.
Lauchertgraben Fault 6
Lauchertgraben Störung 6
WNW-ESE striking normal fault, dipping SSW with unknown angle; southern lateral fault of the Lauchertgraben.
Bad Gögging Fault
Bad Gögging Störung
Inferred from the linear array of subthermal sulfurous springs at Bad Gögging and Irnsing, WNW-ESE striking continuation of Abensberg-Rottenburg Fault [DE-BY_812].
Aus der linearen Anordnung subthermaler Schwefelquellen in Bad Gögging und Irnsing geschlossene, WNW-ESE streichende Fortsetzung der Abensberg-Rottenburg Störung [DE-BY_812].
Irading-Kugelgraben Fault
Iradinger Bruch
Irading-Kugelgraben Störung
Kinked NW-SE to N-S trending, steeply (85°-60°) NE to E dipping normal fault NW to SE of Grasslfing, featuring a throw of up to 20 m.
Nordwestlich bis südöstlich von Graßlfing geknickt NW-SE bis N-S verlaufende, steil (85°-60°) nach NE bis E einfallende Abschiebung mit einem Vertikalversatz bis zu 20 m.
Grossberg Fault
Großberger Verwerfung
Großberg Störung
Running from the Danube river to Niedergebrachting, kinked NW-SE to NNW-SSE trending, steeply (85°-60°) NE to ENE dipping normal fault featuring a throw of up to 30 m.
Von der Donau bis nach Niedergebraching geknickt NW-SE bis NNW-SSE verlaufende, steil (85°-60°) nach NE bis ENE einfallende Abschiebung mit bis zu 30 m Vertikalversatz.
Lower Bavaria - Upper Austria Molasse Basin Eastern Margin Fault Systems
Niederbayerisch-oberösterreichisches Molassebecken Ostrand-Störungssysteme
Foreland Molasse Southern Margin Faults
Südrand-Störungen der Vorlandmolasse
Between Lake Constance in the west and Chiemsee in the east the southern boundary ot the Foreland Molasse is formed by the northern boundary of Subalpine (Folded) Molasse [DE-BY_789]. East of Chiemsee, where the Subalpine Molasse is overthrusted by Alpine units, the Alpine Basal Thrust (Thrust Front of Helvetic, Penninic and Austroalpine Nappes) [DE-BY_753] represents the southern boundary of the Foreland Molasse.
Zwischen dem Bodensee im Westen und dem Chiemsee im Osten wird der Südrand der Vorlandmolasse vom Nordrand der Faltenmolasse (Subalpinen Molasse) [DE-BY_789 gebildet. Östlich des Chiemsees, wo die Subalpine Molasse von den alpinen Einheiten überfahren wurde, bildet die Überschiebungsfront des helvetischen, penninischen und ostalpinen Deckenstapels [DE-BY_753] die Südgrenze der Vorlandmolasse.
Nordrand der Aufgerichteten Molasse
Northern Boundary of Subalpine Molasse
Northern Limit of Tilted Molasse
Northern Boundary of Folded Molasse
Nordrand der subalpinen Molasse
Nordrand der Faltenmolasse
Southern boundary of the Alpine Foreland Molasse towards the Subalpine (aka Folded or Imbricate) Molasse. Commonly WSW-ENE trending, steeply (85°-60°) S dipping reverse fault, laterally displaced by few sinistral transverse faults [DE-BY_788], [DE-BY_933]. Represents the sheared off northernmost flanks of the synclines formed by compressional stress of the Alpine northward thrust. In the western part (Allgäu), where the Folded or Imbricate Molasse merges into tectonic wedging forming triangle zones, it represents the N dipping leg at the crest of the blind, protruding wedges. In the Alpine foothills of eastern Bavaria and Austria the Subalpine Molasse is completely overthrusted by the Alpine nappes, headed by Helvetic nappes and the Rhenodanubian Flysch, thus does not emerge here.
Südgrenze der alpinen Vorlandmolasse. WSW-ENE verlaufende, steil (85°-60°) südwärts einfallende Aufschiebungen, bereichsweise durch N-S verlaufende sinistrale Blattverschiebung [DE-BY_788], [DE-BY_933] versetzt. Wird von den auf die Vorlandmolasse aufgeschobenen Nordflügeln von Muldenstrukturen gebildet, die aus der Kompressionstektonik des nordwärts gerichteten Alpenschubs resultiert. Im Westen (Allgäu), wo die Faltenmolasse in sog. Triangel Zonen übergeht, wird die Grenze vom nordfallenden Schenkel im Scheitel der überdeckten Orogen-Keile aufgebaut. Im Osten der bayerischen Voralpen und in Österreich wurde die Faltenmolasse komplett von den alpinen Decken, zuvorderst Helvetikum und Rhenodanubischer Flysch, überfahren und tritt daher hier nicht zutage.
SW-NE trending fault with left-lateral movement running parallel to the Loisach valley. Displaces the Alpine Basal Thrust [DE-BY_753] and assumedly (not disclosed) the Northern Boundary of Subalpine Molasse [DE-BY_789].
SW-NE verlaufende Störung sub-parallel zum Loisachtal mit sinistral seitenverschiebender Kinematik; versetzt die Alpine Deckenfront [DE-BY_753] und vermutlich (nicht aufgeschlossen) den Nordrand der Faltenmolasse [DE-BY_789].
Loisach Valley Fault System
Penzberg Transfer Fault
Penzberger Querstörung
Loisach Störung
Loisachtal Störungssystem
Southern Boundary of Subalpine Molasse
Alpine Basal Thrust
Südrand der subalpinen Molasse
Alpine Deckenfront
Überschiebungsfront des helvetischen, penninischen und ostalpinen Deckenstapels
Nordgrenze des helvetischen, penninischen und ostalpinen Deckenstapels und Südgrenze der gefalteten Molasse. WSW-ENE verlaufende Überschiebung mit steilem (85°-60°) Süd-Fallen, bereichsweise saiger oder überkippt.
Northern boundary of the Helvetic, Penninic and Austroalpine nappes and southern boundary of Subalpine Molasse. WSW-ENE trending thrust fault with a steep (85°-60°) southerly to vertical dip, in parts recumbent.
Thrust Front of Helvetic, Penninic and Austroalpine Nappes
Molasseflexur
Malm-Abbruch
Due to the lack of prospectivity in terms of hydrocarbon deposits or geothermal potential, very few seismic surveys have been carried out in the shallow parts of the Molasse Basin. Unlike the tectonic boundaries in the deeper parts of the basin, these blind faults are inferred from borehole correlation of the top of Upper Jurassic and the extrapolation of mapped or inferred faults in the respective exposed sequence of the Swabian-Franconian Alb cuesta.
Array of overall SW-NE to W-E trending, steeply SE to S dipping normal faults, in larger sections as step faults or occasionally displaced by lateral faults, running from Ulm / Neu-Ulm to Ingolstadt. The eastward continuation to Neustadt/Donau and Abensberg (Freyberg 1969) is uncertain but, further to the east, seems to be manifested by the Neustadt Flexure between Neustadt/Donau and Bad Gögging (Schmidt-Kaler 1968). To the west of Ulm, a flexure is continuously formed on the northern edge of the Molasse Basin (DE-BW_915], but it does not coincide with the basin edge (the cliff line north of it) (Geyer et al. 2011).
Von Ulm / Neu-Ulm bis Ingolstadt insgesamt SW-NE bis W-E verlaufendes System steil nach Süd bis Südost einfallender Abschiebungen, abschnittsweise als Staffelbruch oder vereinzelt durch Querbrüche versetzt. Eine Fortsetzung nach Osten hin, bis Neustadt/Donau und Abensberg (Freyberg 1969) ist unsicher, scheint sich aber im Osten in der Neustädter Flexur zwischen Neustadt/Donau und Bad Gögging (Schmidt-Kaler 1968) abzuzeichnen. Westlich von Ulm, ist am Molassebecken-Nordrand durchgehend eine Flexur ausgebildet [DE-BW_915], die jedoch nicht mit dem Beckenrand (der Klifflinie nördlich davon) zusammenfällt (Geyer et al. 2011).
Molasse Basin Northern Margin Fault System
Molassebecken-Nordrand Störungssystem
Von Ulm / Neu-Ulm bis Ingolstadt insgesamt SW-NE bis W-E verlaufendes System steil nach Süd bis Südost einfallender Abschiebungen, abschnittsweise als Staffelbruch oder vereinzelt durch Querbrüche versetzt. Eine Fortsetzung nach Osten hin, bis Neustadt/Donau und Abensberg (Freyberg 1969) ist unsicher, scheint sich aber im Osten in der Neustädter Flexur zwischen Neustadt/Donau und Bad Gögging (Schmidt-Kaler 1968) abzuzeichnen.
Alb-Südrandbruch
Franconian Alb Boundary System
Jurarandbruch System
Array of steeply (85°-60°) S to SE dipping normal faults running from Ulm / Neu-Ulm to Ingolstadt; step fault in the Leipheim-Donauwörth area. The eastward continuation to south of Vohburg is uncertain (Jung et al. 2003).
Von Ulm / Neu-Ulm bis Ingolstadt ziehendes System steil nach Süd bis Südost einfallender Abschiebungen, im Bereich Leipheim-Donauwörth als Staffelbruch. Eine Fortsetzung nach Osten hin, bis südlich von Vohburg, ist unsicher (Jung et al. 2003).
Elchingen-Neuburg Fault
Elchingen-Neuburg Störung
WSW-ENE to W-E trending, steeply (85°-60°) SSE to S dipping synthetic normal fault featuring a throw of up tp 50 m; northern and principal subfault of the step fault forming the buried Franconian Alb Boundary System in the Leipheim-Donauwörth area, probably continuing to Ulm / Neu-Ulm in the west and reaching to Neuburg-Fault [DE-BY_1249] in the east.
WSW-ENE bis W-E verlaufende, steil (85°-60°) nach SSE bis S einfallende synthetische Abschiebung; nördliche Teilstörung des überdeckten Jurarand-Staffelbruchs im Bereich Leipheim-Donauwörth, die im Westen wohl bis nach Ulm / Neu-Ulm fortsetzt und im Osten bis zur Neuburg-Störung [DE-BY_1249] reicht.
Lauingen-Schwennigen Subfault
Lauingen-Schwenningen Nebenstörung
WSW-ENE strikng, steeply (85°-60°) SSE dipping synthetic normal fault forming a pre-step of Elchingen-Neuburg Fault.
WSW-ENE streichende, steil (85°-60°) nach SSE einfallende synthetische Abschiebung als Vorstufe der Elchingen-Neuburg Störung.
Moos-Sinning Fault
Moos-Sinning Querstörung
Southwestern boundary of the Neuburg Jurassic spur truncating Nersingen-Sinning Fault [DE-BY_781].
Südwestliche Begrenzung des Neuburger Jura Sporns und östliches Ende der Nersingen-Sinning Störung [DE-BY_781].
WSW-ENE trending, steeply (85°-60°) ± SSE dipping synthetic normal fault running probably from Neu-Ulm, evidenced by borehole correlation from Nersingen, in the west to Sinning in the east, featuring a throw of up to 60 m; middle subfault of the step fault forming the blind Franconian Alb Boundary System in the Leipheim-Donauwörth area.
WSW-ENE verlaufende, steil (85°-60°) nach ± SSE einfallende synthetische Abschiebung, wahrscheinlich zwischen Neu-Ulm (mittels Bohrloch-Korrelation nachgewiesen ab Nersingen) und Sinning, mit einer Sprunghöhe bis zu 60 m; mittlere Teilstörung des überdeckten Jurarand-Staffelbruchs im Bereich Leipheim-Donauwörth.
Nersingen-Sinning Fault
Nersingen-Sinning Störung
Strass-Nordendorf Fault
Strass-Nordendorf Störung
WSW-ENE to W-E trending, steeply (85°-60°) SSE to S dipping synthetic normal fault featuring a throw of up to 50 m; southern subfault of the step fault forming the buried Franconian Alb Boundary System in the Leipheim-Donauwörth area.
WSW-ENE bis W-E verlaufende, steil (85°-60°) nach SSE bis S einfallende synthetische Abschiebung mit einer Sprunghöhe bis zu 50 m; südliche Teilstörung des überdeckten Jurarand-Staffelbruchs im Bereich Leipheim-Donauwörth.
Jurarandbruch
WNW-ESE trending, steeply (85°-60°) SSW dipping normal fault with a throw of up to 80 m between Joshofen NE Neuburg and Hundszell S of Ingolstadt City. Blind fault within the Ingolstadt subbasin, presumably part of the larger, buried section of the Franconian Alb Boundary System continuing to the east (Unger 1999).
Überdeckte WNW-ESE streichende, steil (85°-60°) nach SSW einfallende Abschiebung zwischen Joshofen nordöstlich von Neuburg und Hundszell südlich der Altstadt von Ingolstadt. Die Störung mit einem Versatz von bis zu 80 m verläuft durch das Ingolstädter Becken und ist mutmaßlich Teil eines größeren, überdeckten Abschnitts des Jurarandbruchs der sich nach Osten hin fortsetzt (Unger 1999).
Neuburg Fault
Neuburg Störung
SW-NE striking, steeply (85°-60°) SE dipping normal fault subcropping E to NE of Neuburg/Donau. Southwestern boundary of the Neuburg Jurassic protrudion with Ingolstadt subbasin having a throw of more than 250 m at the top of Jurassic as inferred from correlation of marker horizons (Fiebig & Pürner 2003).
Überdeckte, SW-NE streichende, steil (85°-60°) nach SE einfallende Abschiebung östlich bis nordöstlich von Neuburg a.d. Donau; südöstliche Begrenzung des Neuburger Jurasporns. Aus der Korrelation von Leithorizonten lässt sich zwischen der jurassischen Schichtoberfläche des Neuburger Sporns und des Ingolstädter Beckens eine Sprunghöhe von über 250 m ableiten (Fiebig & Pürner 2003).
Wittislingen-Lutzingen Fault
Wittislingen-Lutzingen Störung
Southeastward arcuate, overall SW-NE trending, steeply (85°-60°) SSE to SE dipping normal fault branch of Mödingen Fault [DE-BY_1254].
Südostwärts gebogen, insgesamt SW-NE verlaufende, steil (85°-60°) nach SSE bis SE einfallende Abschiebung; Abzweig des Mödinger Abbruchs [DE-BY_1254].
Langenau-Wittislingen Fault
Langenau-Wittislingen Störung
WSW-ENE trending, steeply (85°-60°) SSE dipping normal fault subcropping northward parallel to Elchingen-Neuburg Fault [DE-BY_1247] and merging into Riedheim-Wittislingen Fault [DE-BY_1250], continuing northeastward as Mödingen Fault [DE-BY_1254].
WSW-ENE verlaufende, steil (85°-60°) nach SSE einfallende Abschiebung nördlich parallel zur Elchingen-Neuburg Störung [DE-BY_1247]. Geht in die Riedheim-Wittislingen Störung [DE-BY_1250] über, die sich nordostwärts als Mödinger Abbruch [DE-BY_1254] fortsetzt.
Riedheim-Wittislingen Fault
Riedheim-Wittislingen Störung
SW-NE trending, steeply (85°-60°) SE dipping branch of Elchingen-Neuburg Fault [DE-BY_1247]; continuing northeastward as Mödingen Fault [DE-BY_1254].
SW-NE verlaufender, steil (85°-60°) nach SE einfallender Abzweig der Elchingen-Neuburg Störung [DE-BY_1247]; setzt sich nordostwärts im Mödinger Abbruch [DE-BY_1254] fort.
Alb Southern Margin Flexure
Struktureller Nordrand des Molasse Beckens als tektonische Region, welcher jedoch nicht mit dem Beckenrand (bzw. der Klifflinie nördlich davon) zusammenfällt. Im Anschluss an das „Jurarandbruch Sytem“ [DE-BY_1245] östlich von Ulm, ist am Nordrand des Molassebeckens in Baden-Württemberg durchgehend eine Flexur ausgebildet, an der sich die Schichtlagerung des Tafeldeckgebirges auf kurze Distanz von höchstens ca. 1° im Ostteil des südlichen Schichtstufenlandes auf etwa 5° erhöht.
Albsüdrandflexur
Structural northern margin of the Molasse Basin as a tectonic region, which does not coincide with the basin edge (or the cliff line north of it). Following the "Franconian Alb Boundary System" [DE-BY_1245] east of Ulm, a flexure is continuously formed on the northern margin of the Molasse Basin in Baden-Württemberg, where the dip of the overburden increase over a short distance from less than 1° southeast to approx. 5° at most.
Molasse Flexure
Central Foreland Molasse Basin limits and internal faults
Central Foreland Molasse Basin fault domain
All faults of the Central Molasse Basin are blind faults 3D modelled based on evidence of seismic surveys and deep drillings. The concepts refer to the fault traces on the top of Upper Jurassic carbonate sequence (resp. the top of Purbeck) as one of the principal reflectors in seismic surveys. Tectonic boundaries featuring throws of less than approximately 10 m, likewise soft links between faults, like relay ramps or horsetail splays, commonly are subseismic in legacy surveys and detectable only in novel 3D-seismics as carried out in few focus areas. The inventory of concepts, thus, cannot be complete with respect to these features, reflects the state of knowledge as of 2020 and is subject to future amendments.
Alle Störungen im zentralen Molassebecken sind überdeckte Störungen, die im 3D-Modell aus seismischen Messungen sowie Bohrungsbelegen abgeleitet wurden. Die Konzepte der tiefliegenden Störungen im Molassebecken beziehen sich auf die im 3D-Modell ermittelten Schnittspuren an der Oberfläche der Weißjura (einschl. Purbeck) Karbonat-Abfolge. Tektonische Grenzflächen mit Sprunghöhen von weniger als ca. 10 m, gleichermaßen Übergänge zwischen Störungen wie Relais Rampen (relay ramps) oder Auffiederungen (horsetail splays), sind in älteren seismischen Erkundungen gemeinhin nicht erkennbar (subseismisch) und nur in moderner, in wenigen Schwerpunktbereichen durchgeführter 3D-Seismik identifizierbar. Dementsprechend bleibt die Zusammenstellung, Stand 2020, im Hinblick auf solche Phänomene unvollständig und ist Gegenstand künftiger Fortschreibungen.
Zentrales Vorland-Molassebecken Störungs-Domäne
The central part of the South German Molasse Basin, overlapping the territories of Baden-Württemberg and Bavaria, is characterized by syn- and antithetic normal faults related to flexure-like strain of the foreland basin. Faults, often arranged as trains of faults, predominantly trend subparallel to the basin’s centerline and the Alpine Thrust Front. Close to the Landshut-Neuötting crystalline rise the faults’ strike is deflected subparallel to the counterfort of the northward Alpine thrust. All faults of the basin are blind faults, active until Badenian of mid-Miocene at the latest, solely evidenced by seismic surveys and deep drillings.
Für den zentralen Teil des süddeutschen Molassebeckens, der Gebiete in Baden-Württemberg und Bayern einnimmt, sind beckenparallele syn- und antithetische Abschiebungen kennzeichnend, die auf eine flexurartige Dehnung des Vorlandbeckens zurückzuführen sind. Die Störungen verlaufen, oft als Störungszug, subparallel zur Beckenachse und zur alpinen Überschiebungsfront. In der Nähe zum Landshut-Neuöttinger Hoch, ist die Streichrichtung der Störungen subparallel zu diesem Widerlager für den nordwärts gerichteten Alpenschub abgelenkt. Alle Störungen im süddeutschen Molassebecken sind überdeckte Störungen, die bis höchstens ins Badenium (mittleres Miozän) aktiv waren, und nur durch seismische Untersuchungen und tiefe Bohrungen nachgewiesen sind.
Lauchdorf-Bad Wörishofen Fault
Lauchdorf-Bad Wörishofen Störung
SSW-NNE striking, approx. 80° WNW dipping antithetic normal fault running subparallel to synthetic Warmisried-Altensteig Fault [DE-BY_1121] forming a local graben structure.
SSW-NNE streichende, ca. 80° nach WNW einfallende antithetische Abschiebung. Bildet mit der subparallel verlaufenden synthetischen Warmisried-Altensteig Störung [DE-BY_1121] eine lokale Grabenstruktur.
N-S streichende, ca. 80° nach E einfallende Abschiebung.
N-S striking, approx. 80° E dipping normal fault
W-E streichende, ca. 80° nach S einfallende Abschiebung.
W-E striking, approx. 80° S dipping normal fault
W-E streichende, fast saiger stehende Abschiebung.
W-E striking, almost vertical normal fault
WNW-ESE streichende, ca. 70° nach SSW einfallende Abschiebung.
WNW-ESE striking, approx. 70° SSW dipping normal fault
Pfaffenhofen Step Fault
Pfaffenhofener Bruchstaffel
Staggered array of 4 (sub-)parallel W-E to SW-NE striking, steeply (85°-60°) N to NNW dipping antithetic fault scarps with a minor throw immediate north of synthetic Ilmmünster Step Fault [DE-BY_917]. Beyond the four detected faults featuring throws of more than about 10 m, more subseismic fault scarps are possible.
Bruchstaffel aus vier (sub)parallelen, W-E bis SW-NE verlaufenden, steil (85°-60°) nach N bis NNW einfallenden antithetischen Abschiebungen mit geringer Sprunghöhe, unmittelbar nördlich der synthetischen Ilmmünster Bruchstaffel [DE-BY_917]. Neben den vier identifizierbaren Stufen mit Sprunghöhen von mehr als ca. 10 m sind weitere subseismische Bruchstufen möglich.
Bad Wörishofen Fault
Bad Wörishofen Störung
WNW-ESE striking, approx. 85° SSW dipping synthetic normal fault.
WNW-ESE streichende, ca. 85° nach SSW einfallende synthetische Abschiebung.
Pless-Winterrieden Fault
Pleß-Winterrieden Störung
SW-NE striking, steeply (85°-60°) SE dipping synthetic normal fault.
SW-NE streichende, steil (85°-60°) nach SE einfallende synthetische Abschiebung.
Fellheim-Oberschönegg Fault
Fellheim-Oberschönegg Störung
WSW-ENE striking, approx. 55° SSE dipping synthetic normal fault.
WSW-ENE streichende, in etwa 55° nach SSE einfallende synthetische Abschiebung.
Kellmünz Fault
Kellmünz Störung
SW-NE striking, approx. 70° SE dipping synthetic normal fault connecting into Baden-Württembergian territory.
SW-NE streichende, in etwa 70° nach SE einfallende synthetische Abschiebung mit Fortsetzung in Baden-Württemberg.
Ichenhausen-Zusmarshausen Fault
Ichenhausen-Zusmarshausen Störung
Mainly WSW-ENE striking, veering to a WNW-ESE trend in its eastern part, steeply (85°-60°) NNW to NNE dipping antithetic normal fault.
Überwiegend WSW-ENE streichende, im Ostteil auf WNW-ESE drehende, steil (85°-60°) nach NNW bis NNE einfallende antithetische Abschiebung.
Ellzee-Scheppach Fault
Ellzee-Scheppach Störung
SSW-NNE striking, steeply (85°-60°) NNW dipping antithetic normal fault, branch of Ichenhausen-Zusmarshausen Fault [DE-BY_785].
SSW-NNE streichende, steil (85°-60°) nach NNW einfallende antithetische Abschiebung, Zweig der Ichenhausen-Zusmarshausen Störung [DE-BY_785].
Ichenhausen Subfault
Ichenhausen Nebenstörung
Branch of Ichenhausen-Zusmarshausen Fault. SSW-NNE striking, steeply (85°-60°) WNW dipping antithetic normal fault.
Zweig der Ichenhausen-Zusmarshausen Störung. SSW-NNE streichende, steil (85°-60°) nach NNW einfallende antithetische Abschiebung.
Kirchberg-Osterberg Fault
Kirchberg-Osterberg Störung
WSW-ENE striking, approx. 70° SSE dipping synthetic normal fault connecting into Baden-Württembergian territory.
WSW-ENE streichende, in etwa 70° nach SSE einfallende synthetische Abschiebung mit Fortsetzung in Baden-Württemberg.
Derching-Wollomoos Fault
Derching-Wollomoos Störung
Mainly WSW-ENE trending, veering to an undulate WNW-ESE trend in its eastern part, steeply (85°-60°) NNW to NNE dipping antithetic normal fault.
Überwiegend WSW-ENE verlaufende, im Ostteil wellenförmig auf WNW-ESE drehende, steil (85°-60°) nach NNW bis NNE einfallende antithetische Abschiebung.
Klingen Subfault
Klingen Nebenstörung
W-E striking, steeply (85°-60°) N dipping antithetic normal fault.
W-E streichende, steil (85°-60°) nach N einfallende antithetische Abschiebung.
Neusäss-Aichach Fault
Neusäß-Aichach Störung
WSW-ENE trending, steeply (85°-60°) S dipping synthetic normal fault.
WSW-ENE verlaufende, steil (85°-60°) nach S einfallende synthetische Abschiebung.
Illertissen-Messhofen Fault
Illertissen-Meßhofen Störung
WSW-ENE to SW-NE striking, steeply (85°-60°) ± NW dipping antithetic normal fault.
WSW-ENE bis SW-NE streichende, steil (85°-60°) nach ± NW einfallende antithetische Abschiebung.
Matzenhofen Cross-fault
Matzenhofen Querstörung
NW-SE striking, approx. 80° NE dipping antithetic normal fault, cross-fault to Illertissen-Messhofen Fault [DE-BY_871].
NW-SE streichende, in etwa 80° nach NE einfallende antithetische Abschiebung; Querstörung zur Illertissen-Meßhofen Störung [DE-BY_871]
Altenstadt-Buch Fault
Altenstadt-Buch Störung
SW-NE striking, steeply (85°-60°) NW dipping antithetic normal fault, branch of Illertissen-Messhofen Fault [DE-BY_871].
SW-NE streichende, steil (85°-60°) nach NW einfallende antithetische Abschiebung; Zweig der Illertissen-Meßhofen Störung [DE-BY_871].
Vöhringen-Roggenburg Fault
Vöhringen-Roggenburg Störung
WNW-ESE striking, steeply (85°-60°) NNE dipping antithetic normal fault.
WNW-ESE streichende, steil (85°-60°) nach NNE einfallende antithetische Abschiebung.
Zusmarshausen-Gundelsdorf Fault
Zusmarshausen-Gundelsdorf Störung
Undulate, overall WSW-ENE trending, steeply (85°-60°) ± NNW dipping antithetic normal fault.
WSW-ENE verlaufende, steil (85°-60°) nach NNW einfallende antithetische Abschiebung.
Adelsried-Aichach Subfault
Adelsried-Aichach Störung
Southern branch of Zusmarshausen-Gundelsdorf Fault [DE-BY_777]. Undulate, overall W-E trending, steeply (85°-60°) ± N dipping antithetic normal fault running from Adelsried to Kühbach.
Wellenförmig insgesamt W-E verlaufende, steil (85°-60°) nach ± N einfallende antithetische Abschiebung. Südlicher, von Adelsried bis Kühbach verlaufender Ast der Zusmarshausen-Gundelsdorf Störung.
WSW-ENE streichende, fast saiger stehende Abschiebung.
[lca_012]
WSW-ENE striking, almost vertical normal fault
[lca_014]
SW-NE striking, approx. 65° NW dipping normal fault
SW-NE streichende, ca. 65° nach NW einfallende Abschiebung.
WNW-ESE streichende, ca. 75° nach NNE einfallende Abschiebung.
[lca_015]
WNW-ESE striking, approx. 75° NNE dipping normal fault
[lca_082]
WSW-ENE streichende, ca. 85° nach SSE einfallende Abschiebung.
WSW-ENE striking, approx. 85° SSE dipping normal fault
[lca_010]
WSW-ENE striking, approx. 60° NNW dipping normal fault.
WSW-ENE streichende, ca. 60° nach NNW einfallende Abschiebung.
Unterbergen-Althegnenberg Fault
Unterbergen-Althegnenberg Störung
W-E striking, approx. 75° S dipping synthetic normal fault.
W-E streichende, ca. 75° nach S einfallende synthetische Abschiebung.
SW-NE trending, approx. 70° NW dipping normal fault
SW-NE streichende, ca. 70° nach NW einfallende Abschiebung.
WSW-ENE striking, approx. 60° SSE dipping normal fault
[lca_016]
WSW-ENE streichende, ca. 60° nach SSE einfallende Abschiebung.
WSW-ENE streichende, ca. 65° nach SSE einfallende Abschiebung.
[lca_017]
WSW-ENE striking, approx. 65° SSE dipping normal fault
[lca_018]
SW-NE bis SSW-NNE streichende, ca. 60° nach SE einfallende Abschiebung.
SW-NE to SSW-NNE trending, approx. 60° SE to ESE dipping normal fault
SW-NE striking, approx. 65° SE dipping normal fault
SW-NE streichende, ca. 65° nach SE einfallende Abschiebung.
SSW-NNE streichende, ca. 55° nach ESE einfallende Abschiebung.
SSW-NNE striking, approx. 55° ESE dipping normal fault
[lca_019]
Eurasburg-Gartenberg Fault
Eurasburg-Gartenberg Störung
WSW-ENE striking, approx. 85° NNW dipping antithetic normal fault.
WSW-ENE streichende, ca. 85° nach NNW einfallende antithetische Abschiebung.
Puchheim-Feldmoching Fault
Puchheim-Feldmoching Störung
SW-NE trending, approx. 75° SE dipping synthetic normal fault west to north of Munich.
SW-NE verlaufende, ca. 75° nach SE einfallende synthetische Abschiebung im Westen bis Norden von München.
Langenneufnach-Döpshofen Fault
Langenneufnach-Döpshofen Störung
WSW-ENE striking, approx. 65° NNW dipping antithetic normal fault.
WSW-ENE streichende, ca. 65° nach NNW einfallende antithetische Abschiebung.
Alling-Lochhausen Fault
Alling-Lochhausen Störung
SW-NE striking, approx. 80° SE dipping synthetic normal fault west to northwest of Munich.
SW-NE streichende, ca. 80° nach SE einfallende synthetische Abschiebung im Westen bis Nordwesten von München.
Wollmetshofen-Leitershofen Fault
Wollmetshofen-Leitershofen Störung
WSW-ENE striking, approx. 80° NNW dipping antithetic normal fault.
WSW-ENE streichende, ca. 80° nach NNW einfallende antithetische Abschiebung.
Erding-Altfraunhofen Fault
Erding-Altfraunhofen Störung
SW-NE trending, on av. approx. 65° SE dipping synthetic normal fault. In the area of Erding running subparallel to antithetic Erding Subfault [DE-BY_1134] forming a local graben structure.
SW-NE verlaufende, im Mittel ca. 65° nach SE einfallende synthetische Abschiebung. Bildet im Raum Erding mit der südlich subparallel verlaufenden, antithetischen Erding Nebenstörung [DE-BY_1134] eine lokale Grabenstruktur.
Oberding Subfault
Oberding Nebenstörung
W-E striking approx. 80° S dipping synthetic normal fault.
W-E streichende, ca. 80° nach S einfallende synthetische Abschiebung.
Faistenhaar-Egmating Fault
Faistenhaar-Egmating Störung
WSW-ENE striking, approx. 75° SSE dipping synthetic normal fault running parallel to Sauerlach-Schlacht Fault [DE-BY_1199] in the south.
WSW-ENE streichende, ca. 75° nach SSE einfallende synthetische Abschiebung parallel zur Sauerlach-Schlacht Störung [DE-BY_1199] unmittelbar südlich.
Argelsried-Planegg Fault
Argelsried-Planegg Störung
W-E striking, approx. 85° N dipping antithethic normal fault forming a local graben structure with synthetic Gilching-Planegg Fault [DE-BY_1128] paralleling to the north.
W-E streichende, ca. 85° nach N einfallende antithetische Abschiebung. Bildet mit der nördlich parallel verlaufenden synthetischen Gilching-Planegg Störungen [DE-BY_1128] eine lokale Grabenstruktur.
Sauerlach-Schlacht Fault
Sauerlach-Schlacht Störung
Undulate WSW-ENE trending, averaged approx. 75° SSE dipping synthetic normal fault
Gewellt WSW-ENE verlaufende, ca. 75° nach SSE einfallende synthetische Abschiebung.
Gilching-Planegg Fault
Gilching-Planegg Störung
W-E striking, approx. 70° S dipping synthethic normal fault forming a local graben structure with antithetic Argelsried-Planegg Fault [DE-BY_1129] paralleling to the south.
W-E streichende, ca. 70° nach S einfallende synthetische Abschiebung. Bildet mit der südlich parallel verlaufenden antithetischen Argelsried-Planegg Störungen [DE-BY_1129] eine lokale Grabenstruktur.
Frasshausen Fault
Fraßhausen Störung
WNW-ESE striking, approx. 80° SSW dipping synthetic normal fault.
WNW-ESE streichende, ca. 80° nach SSW einfallende synthetische Abschiebung.
Gilching-Germering Fault
Gilching-Germering Störung
WSW-ENE striking, approx. 80° SSE dipping synthethic normal fault.
WSW-ENE streichende, ca. 80° nach SSE einfallende synthetische Abschiebung.
Thanning Fault
Thanning Störung
WSW-ENE striking, approx. 65° SSE dipping synthetic normal fault.
WNW-ESE streichende, ca. 65° nach SSE einfallende synthetische Abschiebung.
Hadern-Laim Fault
Hadern-Laim Störung
WSW-ENE striking, approx. 75° NNW dipping antithethic normal fault underpassing the western precincts of Munich city center.
WSW-ENE streichende, ca. 75° nach NNW einfallende antithetische Abschiebung im Westen der Münchener Innenstadt.
Föggenbach Fault
W-E striking, approx. 75° N dipping antithetic normal fault running parallel to Humbach-Dietenhausen Fault [DE-BY_1195] in the south.
W-E streichende, ca. 75° nach N einfallende antithetische Abschiebung parallel zur Humbach-Dietenhausen Störung [DE-BY_1195] unmittelbar südlich.
Föggenbach Störung
Pasing-Daglfing Fault
Pasing-Daglfing Störung
W-E trending, approx. 60° ± S dipping synthetic normal fault underpassing the northern precincts of Munich city center.
W-E verlaufende, ca. 60° nach ± S einfallende synthetische Abschiebung im Norden der Münchener Innenstadt.
Humbach-Dietenhausen Fault
Humbach-Dietenhausen Störung
W-E striking, approx. 75° N dipping antithetic normal fault running parallel to Föggenbeuren Fault [DE-BY_1196] in the north.
W-E streichende, ca. 75° nach N einfallende antithetische Abschiebung parallel zur Föggenbeuren Störung [DE-BY_1196] unmittelbar nördlich.
Schwabing Fault
Schwabing Störung
WNW-ESE trending, approx. 70° SSW dipping synthetic normal fault underpassing the north of Munich.
WNW-ESE verlaufende, ca. 70° nach SSW einfallende synthetische Abschiebung im Norden Münchens.
Babenstuben-Sachsenkam Fault
Babenstuben-Sachsenkam Störung
WNW-ESE striking, approx. 70° NNE dipping antithetic normal fault.
WNW-ESE streichende, ca. 70° nach NNE einfallende antithetische Abschiebung.
Milbertshofen Fault
Milbertshofen Störung
WSW-ENE striking, approx. 80° SSE dipping synthetic normal fault in the north of Munich.
WSW-ESE streichende, ca. 80° nach SSE einfallende synthetische Abschiebung im Norden von München.
SSW-NNE streichende, ca. 70° nach ESE einfallende Abschiebung.
[lca_023]
SSW-NNE striking, approx. 70° ESE dipping normal fault
[lca_025]
SW-NE striking, approx. 75° SE dipping normal fault
SW-NE streichende, ca. 75° nach SE einfallende Abschiebung.
WSW-ENE striking, approx. 80° SSE dipping normal fault
WSW-ENE streichende, ca. 80° nach SSE einfallende Abschiebung.
[lca_026]
NW-SE striking, approx. 60° NE dipping normal fault
NW-SE streichende, ca. 60° nach NE einfallende Abschiebung.
[lca_020]
[lca_021]
SW-NE streichende, ca. 80° nach SE einfallende Abschiebung.
SW-NE striking, approx. 80° SE dipping normal fault
SW-NE striking, approx. 70° NW dipping normal fault
WSW-ENE streichende, ca. 70° nach NNW einfallende Abschiebung.
WSW-ENE striking, approx. 70° NNW dipping normal fault
[lca_022]
SW-NE trending, approx. 80° SE dipping normal fault
SSW-NNE striking, approx. 85° WNW dipping normal fault
SSW-NNE streichende, ca. 85° nach WNW einfallende Abschiebung.
WSW-ENE striking, approx. 70° SSE dipping normal fault
WSW-ENE streichende, ca. 70° nach SSE einfallende Abschiebung.
[lca_027]
SW-NE striking, approx. 70° SE dipping normal fault
SW-NE streichende, ca. 70° nach SE einfallende Abschiebung.
Waldhausen-Asten Fault
Waldhausen-Asten Störung
W-E striking, approx. 65° S dipping synthetic normal fault.
W-E streichende, ca. 65° nach S einfallende synthetische Abschiebung.
Halsbach Subfault
Halsbach Nebenstörung
WSW-ENE striking, approx. 70° SSE dipping synthetic normal fault.
WSW-ENE streichende, ca. 70° nach S einfallende synthetische Abschiebung.
Kraiburg-Unterneukirchen Fault
Kraiburg-Unterneukirchen Störung
W-E trending, approx. 65° N dipping antithetic normal fault.
W-E verlaufende, ca. 65° nach N einfallende antithetische Abschiebung.
Jettenbach Fault
Jettenbach Störung
Slightly undulate, overall W-E trending, approx. 75° S dipping synthetic normal fault south of Waldkraiburg.
Leicht gewellt, ingesamt W-E verlaufende, ca. 75° nach S einfallene synthetische Abschiebung südlich von Waldkraiburg.
Guggenberg-Erisried Fault
Guggenberg-Erisried Störung
SW-NE striking, approx. 50° SE dipping synthetic normal fault subparallel to Lautrach-Stetten Fault [DE-BY_849].
SW-NE streichende, ca. 50° nach SE einfallende synthetische Abschiebung subparallel zur Lautrach-Stetten Störung [DE-BY_849],
Arlesried Fault System
Arlesried Störungssystem
Structure of northward arcuate antithetic normal faults confining oil & gas field Arlesried.
Das Öl- und Gasfeld Arlesried begrenzende Struktur aus nordwärts bogenförmig verlaufenden antithetischen Abschiebungen.
Hohenschlau Fault
Hohenschlau Störung
Northward arcuate, overall WSW-WNE trending, steeply (85°-60°) ± NNW dipping antithetic normal fault south of Arlesried Subfault.
Nordwärts bogenförmig, insgesamt WSW-WNE verlaufende, steil (85°-60°) nach ± NNW einfallende antithetische Abschiebung südlich der Arlesried Parallelstörung.
Arlesried Subfault
Arlesried Parallelstörung
Northward arcuate, undulate SW-NE to NW-SE trending, steeply (85°-60°) NW to NE dipping antithetic normal fault southward subparallel to the middle section of Arlesried Fault.
Nordwärts bogenförmig, gewellt SW-NE bis NW-SE verlaufende, steil (85°-60°) nach NW bis NE einfallende antithetische Abschiebung südlich subparallel zum mittleren Abschnitt der Arlesried Störung.
Arlesried Fault
Arlesried Störung
Northern boundary of oil & gas field Arlesried. Northward arcuate SW-NE to NW-SE trending, approx. 75° NW to NE dipping antithetic normal fault running from Egg to Oberrieden.
Nördliche Begrenzung des Öl- und Gasfeldes Arlesried. Nordwärts bogenförmig SW-NE bis NW-SE verlaufende, ca. 75° nach NW bis NE einfallende antithetische Abschiebung mit zwischen Egg und Oberrieden.
Oberrieden Lateral Fault
Oberrieden Querstörung
WSW-ENE trending, steeply (85°-60°) NNW dipping antithetic normal fault merging into the far eastern limp of Arlesried Fault.
WSW-ENE verlaufende, steil (85°-60°) nach NNW einfallende antithetische Abschiebung mit Übergang in den äußeren westlichen Ast der Arlesried Störung.
Weilbach Lateral Fault
Weilbach Querstörung
SSW-NNE trending, steeply (85°-60°) WNW dipping antithetic normal fault merging into the eastern limp of Arlesried Fault.
SSW-NNE verlaufende, steil (85°-60°) nach WNW einfallende antithetische Abschiebung mit Übergang in den West-Ast der Arlesried Störung.
Lautrach-Stetten Fault
Lautrach-Stetten Störung
Overall SW-NE trending, steeply (85°-60°) SE dipping synthetic normal fault running from Iller river to Mindelheim.
Insgesamt SW-NE verlaufende, steil (85°-60°) nach SE einfallende synthetische Abschiebung von der Iller bis nach Mindelheim.
Grossaitingen Fault
Großaitingen Störung
Northern boundary of oil & gas fields Schwabmünchen and Aitingen. W-E striking, approx. 55° N dipping antithetic normal fault north of Schwabmünchen.
Nördliche Begrenzung der Öl- und Gasfelder Schwabmünchen und Aitingen. W-E streichende, ca. 55° nach N einfallende antithetische Abschiebung nördlich von Schwabmünchen.
Lindau-Hergatz Störung
SW-NE striking, approx. 65° SE dipping synthetic normal fault.
SW-NE streichende, ca. 65° nach SE einfallende synthetische Abschiebung.
Lindau-Hergatz Fault
Haimhausen Fault
Haimhausen Störung
Northern boundary of oil- and gasfield Haimhausen. Northward arcuate, overall SW-NE trending, steeply (85°-60°) NNW to NE dipping antithetic normal fault of the same structure as Herbertshausen Fault [DE-BY_740] to the SW.
Nördliche Begrenzung des Öl- und Gasfeldes Haimhausen. Nordwärts gebogene, insgesamt SW-NE verlaufende, steil (85°-60°) nach NNW bis NE einfallende antithetische Abschiebung derselben Struktur wie die SW gelegene Herbertshausen Störung [DE-BY_740].
Boos Fault
Boos Störung
Northern boundary of oil- and gasfield Boos. Northward curved overall W-E trending, steeply (85°-60°) NW to NE dipping antithetic normal fault.
Nördliche Begrenzung des Öl- und Gasfeldes Boos. Nordwärts gebogene, übergeordnet W-E verlaufende, steil (85°-60°) nach NW bis NE einfallende antithetische Abschiebung.
Tylraching Fault
Tyrlaching Störung
W-E to WNW-ESE trending, approx. 65° S to SSW dipping synthetic normal fault.
W-E bis WNW-ESE verlaufende, ca. 65° nach S bis SSW einfallende synthetische Abschiebung.
Lauben-Lauberhart Fault
Lauben-Lauberhart Störung
Northern boundary of oil- and gasfields Lauberhart and Lauben. Arc-shaped SW-NE to NW-SE trending, steeply (85°-60°) NW to NE dipping antithetic normal fault.
Nördliche Begrenzung der Öl- und Gasfelder Lauberhart und Lauben. Bogenförmig SW-NE bis NE-SW verlaufende, steil (85°-60°) nach NW bis NE einfallende antithetische Abschiebung.
Kirchweidach Fault
Kirchweidach Störung
WNW-ESE to NW-SW trending, approx. 70° SSW to SW dipping synthetic normal fault running from Thann to Tittmoning.
WNW-ESE bis NW-SW verlaufende, ca. 70° nach SSW bis SW einfallende synthetische Abschiebung zwischen Thann und Tittmoning.
SW-NE striking, approx. 60° SE dipping normal fault
SW-NE streichende, ca. 60° nach SE einfallende Abschiebung.
SW-NE striking, approx. 80° NW dipping normal fault
SW-NE streichende, ca. 80° nach NW einfallende Abschiebung.
SSW-NNE striking, approx. 75° ESE dipping normal fault
SSW-NNE streichende, ca. 75° nach ESE einfallende Abschiebung.
W-E streichende, ca. 75° nach S einfallende Abschiebung.
W-E striking, approx. 75° S dipping normal fault
SSW-NNE striking, approx. 70° WNW dipping normal fault
SSW-NNE streichende, ca. 70° nach WNW einfallende Abschiebung.
Oberfeldkirchen Fault
Oberfeldkirchen Störung
SSW-NNE streichende, ca. 75° nach WNW einfallende Abschiebung.
SSW-NNE trending, approx. 75° WNW dipping normal fault
Eurishofen-Waal Fault
Eurishofen-Waal Störung
WSW-ENE striking, approx. 80° SSE dipping synthetic normal fault.
Warmisried-Altensteig Fault
Warmisried-Altensteig Störung
SSW-NNE trending, approx. 80° ESE dipping synthetic normal fault running subparallel to antithetic Lauchdorf-Bad Wörishofen Fault [DE-BY_1188] forming a local graben structure.
SSW-NNE ziehende, ca. 80° nach ESE einfallende synthetische Abschiebung. Bildet mit der subparallel verlaufenden antithetischen Lauchdorf-Bad Wörishofen Störung [DE-BY_1188] eine lokale Grabenstruktur.
Unterschweinbach Fault
Unterschweinbach Störung
W-E striking, approx. 65° N dipping antithetic normal fault.
W-E streichende, ca. 65 nach N einfallende antithetische Abschiebung.
Dirlewang-Scheuring Fault
Dirlewang-Scheuring Störung
Slightly undulate, overall SW-NE trending, averaged approx. 75° SE dipping synthetic normal fault running from south of Mindelheim to the Lech river.
Leicht gewellt, insgesamt SW-NE verlaufende, im Mittel ca. 75° nach SE einfallende synthetische Abschiebung zwischen S von Mindelheim und dem Lech.
Wolnzach Fault
Wolnzach Störung
WNW-ESE to NW-SE trending, steeply (85°-60°) NNE to NE dipping antithetic normal fault.
WNW-ESE bis NW-SE verlaufende, steil (85°-60°) nach NNE bis NE einfallende antithetische Abschiebung.
Mindelheim-Türkheim Fault
Mindelheim-Türkheim Störung
E-W trending, approx. 70° N dipping antithetic normal fault.
E-W verlaufende, ca. 70° nach N einfallende antithetische Abschiebung.
Obing-Altenmarkt Fault
Obing-Altenmarkt Störung
W-E trending, approx. 60° S dipping synthetic normal fault.
W-E verlaufende, ca. 60° nach S einfallende synthetische Abschiebung.
Rammingen-Berg Fault
Rammingen-Berg Störung
WSW-ENE streichende, ca. 65° nach SSE einfallende synthetische Abschiebung.
Aham-Stockham Fault
Aham-Stockham Störung
W-E trending, approx. 60° S dipping synthetic normal fault north of Amerang and Obing.
W-E verlaufende, ca. 60° nach S einfallende synthetische Abschiebung nördlich Amerang und Obing.
Tussenhausen-Siebnach Fault
Tussenhausen-Siebnach Störung
WSW-ENE trending, approx. 85° SSE dipping synthetic normal fault.
WSW-ENE streichende, ca. 85° nach SSE einfallende synthetische Abschiebung.
Wasserburg-Schnaitsee Fault
Wasserburg-Schnaitsee Störung
Erlenberg-Tussenhausen Fault
Erlenberg-Tussenhausen Störung
WSW-ENE trending, approx. 60° SSE dipping synthetic normal fault.
WSW-ENE streichende, ca. 60° nach SSE einfallende synthetische Abschiebung.
Lauberhart-Daxberg Fault
Lauberhart-Daxberg Störung
Schnaitsee-Trostberg Fault
Schnaitsee-Trostberg Störung
WNW-ESE trending, approx. 65° SSW dipping synthetic normal fault.
WNW-ESE verlaufende, ca. 65° nach SSW einfallende synthetische Abschiebung.
Schmidham Subfault
Schmidham Nebenstörung
WSW-ENE striking, approx. 70° SSE dipping synthetic normal fault. Branch of Schnaitsee-Trostberg Fault [DE-BY_856].
WSW-ENE streichende, ca. 70° nach SSE einfallende synthetische Abschiebung. Zweig der Schnaitsee-Trostberg Störung [DE-BY_856].
Niederrieden Fault
Niederrieden Störung
Northern boundary of oil- and gasfield Niederrieden. NW-SE trending, steeply (85°-60°) NNE to NE dipping antithetic normal fault.
Nördliche Begrenzung des Öl- und Gasfeldes Niederrieden. NW-SE verlaufende, steil (85°-60°) nach NNE bis NE einfallende antithetische Abschiebung.
W-E streichende, ca. 65° nach N einfallende Abschiebung.
[lca_001]
W-E trending, approx. 65° N dipping normal fault
SW-NE striking, approx. 50° SE dipping normal fault
[lca_029]
SW-NE streichende, ca. 50° nach SE einfallende Abschiebung.
[lca_077]
WNW-ESE striking, approx. 85° NNE dipping normal fault
WNW-ESE streichende, ca. 85° nach NNE einfallende Abschiebung.
[lca_002]
SW-NE streichende, ca. 85° nach SE einfallende Abschiebung.
[lca_004]
SW-NE striking, approx. 85° SE dipping normal fault
Reichertshofen Fault Scarp
Reichertshofener Abbruch
WNW-ESE striking, steeply (85°-60°) SSW dipping synthetic normal fault south of Ingolstadt, possibly the southern fault scarp (resp. step fault) of the Jurarandbruch [DE-BY_1245]. Continuation further to the (south)east, merging into the Landshut-Neuötting Step Fault, is inferred (Jerz & Schmidt-Kaler 1999, Doppler et al. 2002) but not evidenced yet.
WNW-ESE streichende, steil (85°-60°) nach SSW einfallende synthetische Abschiebung südlich von Ingolstadt. Möglicherweise südliche Abbruchstufe (bzw. Bruchstaffel) des Jurarandbruchs [DE-BY_1245]; eine Fortsetzung nach (Süd-)Osten hin mit Übergang in den Landshut-Neuöttinger Abbruch, wird vermutet (Jerz & Schmidt-Kaler 1999, Doppler et al. 2002), konnte aber bisher nicht nachgewiesen werden.
Stockheim-Buchloe Fault
Stockheim-Buchloe Störung
SW-NE trending, approx. 75° SE dipping synthetic normal fault.
SW-NO verlaufende, ca. 75° nach SE einfallende synthetische Abschiebung.
SW-NE trending, approx. 65° SE dipping normal fault
Heimertingen Fault System
Heimertinger Störungsschar
Heimertingen Störungssystem
Structure confining oil and gas field Heimertingen. WSW-ENE and WNW-ESE striking antithetic normal faults with a steep (85°-60°) dip towards NNW, resp. NNE.
Das Öl- und Gasfeld Heimertingen begrenzende Struktur aus WSW-ENE und WNW-ESE streichenden, antithetischen Abschiebungen mit steilem (85°-60°) Einfallen nach NNW bzw. NNE.
[lca_009]
SSW-NNE striking, approx. 65° WNW dipping normal fault
SSW-NNE streichende, ca. 65° nach WNW einfallende Abschiebung.
SW-NE streichende, ca. 60° nach NW einfallende Abschiebung.
SW-NE striking, approx. 60° NW dipping normal fault
SW-NE striking, approx. 75° NW dipping normal fault
SW-NE streichende, ca. 75° nach NW einfallende Abschiebung.
[lca_007]
WNW-ESE striking, approx. 80° NNE dipping normal fault
WNW-ESE streichende, ca. 80° nach NNE einfallende Abschiebung.
Irschenberg Fault
Irschenberg Störung
WSW-ENE streichenede, ca. 80° nach NNW einfallende antithetische Abschiebung.
Utting Fault
Utting Störung
W-E striking, approx. 70° N dipping antithetic normal fault.
W-E streichende, ca. 70° nach N einfallende antithetische Abschiebung.
Eberfing-Eurasburg Fault
Eberfing-Eurasburg Störung
Undulate SW-NE trending, approx. 80° SE dipping synthetic normal fault.
Wellenförmig SW-NE verlaufende, ca. 80° nach SE einfallende synthetische Abschiebung.
Miesbach Fault
Miesbach Störung
Slightly northward arcuate W-E trending, approx. 70° N dipping antithetic normal fault north of Miesbach.
Leicht nordwärts gekrümmte, W-E verlaufende, ca. 70° nach N einfallende antithetische Abschiebung nördlich von Miesbach.
SSW-NNE streichende, ca. 80° nach ESE einfallende Abschiebung.
SSW-NNE striking, approx. 80° ESE dipping normal fault
Deisenhofen-Wächterhof Fault
Deisenhofen-Wächterhof Störung
Markt Oberdorf Fault
Markt Oberdorf Störung
Undulating WSW-ENE trending, approx. 75° NNW dipping antithetic normal fault running from Kempter Wald to Schongau.
Gewellt WSW-ENE verlaufende, ca. 75° nach NNW einfallende antithetische Abschiebung zwischen Kempter Wald und Schongau.
Brunnthal Fault
Brunnthal Störung
WSW-ENE streichende, ca. 85° nach SSE einfallende synthetische Abschiebung; bildet mit der südlich parallel verlaufenden antithetischen Wolfersberg-Moosach Störung [DE-BY_734] eine lokale Grabenstruktur.
WSW-ENE striking, approx. 85° SSE dipping synthetic normal fault parallel to antithetic Wolfersberg-Moosach Fault [DE-BY_734] forming a local graben structure.
Lengenwang Fault
Lengenwang Störung
WSW-ENE trending, approx. 65° NNW dipping antithetic normal fault.
WSW-ENE verlaufende, ca. 65° nach NNW einfallende antithetische Abschiebung.
Wolfersberg-Moosach Fault
Wolfersberg-Moosach Störung
Northern boundary of oil- and gasfields Wolfersberg and Moosach. Undulate WSW-ENE trending, averaged approx. 75° NNW dipping antithetic normal fault running from Sauerlach to Forsting.
Nördliche Begrenzung der Öl- und Gasfelder Wolfersberg und Moosach. Gewellt WSW-ENE verlaufende, im Mittel ca. 75° nach NNW einfallende antithetische Abschiebung zwischen Sauerlach und Forsting.
Lengenwang-Lech Fault
Lengenwang-Lech Störung
WSW-ENE trending, approx. 70° SSE dipping synthetic normal fault.
WSW-ENE verlaufende, ca. 70° nach SSE einfallende synthetische Abschiebung.
Waging-Kirchanschöring Fault
Waging-Kirchanschöring Störung
Undulate W-E trending, approx. 55° N dipping antithetic normal fault.
Wellenförmig W-E verlaufende, ca. 55° nach N einfallende antithetische Abschiebung.
Königsdorf South Fault
Königsdorf Süd Störung
W-E striking, approx. 85° N dipping antithetic normal fault. Subparallel to synthetic Königsdorf North Fault [DE-BY_836], this probably conjugate pair of faults forms a local graben structure.
W-E streichende, ca. 85° nach N einfallende antithetische Abschiebung. Subparallel zur synthetischen Königsdorf Nord Störung [DE-BY_836] bildet dieses wahrscheinlich konjugierte Störungspaar eine lokale Grabenstruktur.
Königsdorf North Fault
Königsdorf Nord Störung
W-E striking, approx. 85° S dipping synthetic normal fault. Subparallel to antithetic Königsdorf South Fault [DE-BY_837], this probably conjugate pair of faults forms a local graben structure.
W-E streichende, ca. 85° nach S einfallende synthetische Abschiebung. Subparallel zur antithetischen Königsdorf Süd Störung [DE-BY_837] bildet dieses wahrscheinlich konjugierte Störungspaar eine lokale Grabenstruktur.
Schondorf Fault
Schondorf Störung
Finning Fault
Finning Störung
W-E striking, approx. 75° N dipping antithetic normal fault.
W-E streichende, ca. 75° nach N einfallende antithetische Abschiebung.
Hebertshausen Fault
Hebertshausen Störung
Northern boundary of oil- and gasfield Hebertshausen. WSW-ENE trending, steeply (85°-60°) NNW dipping antithetic normal fault of the same structure as Haimhausen Fault [DE-BY_741] to the NE.
Nördliche Begrenzung des Öl- und Gasfeldes Hebertshausen. WSW-ENE verlaufende, steil (85°-60°) nach NNW einfallende antithetische Abschiebung derselben Struktur wie die NE gelegene Haimhausen Störung [DE-BY_741].
Bad Aibling Fault
Bad Aibling Störung
SW-NE striking, steeply (85°-60°) NW dipping antithetic normal fault.
SW-NE streichende, steil (85°-60°) nach NW einfallende antithetische Abschiebung.
Schmidhausen-Inzenham-Zaissberg Fault
Schmidhausen-Inzenham-Zaißberg Störung
Northward arcuate structure located nearby oil- and gasfields Schmidhausen and Inzenham-Zaissberg. Overall W-E trending, steeply (85°-60°) NW to NNE dipping antithetic normal fault north of Rosenheim.
Nordwärts gebogene Struktur an den Öl- und Gasfeldern Schmidhausen und Inzenham-Zaissberg. Insgesamt W-E verlaufende, steil (85°-60°) nach NW bis NNE einfallende antithetische Abschiebung nördlich von Rosenheim.
Tattenhausen Fault
Tattenhausen Störung
SW-NE striking, ca. 70° NW dipping antithetic normal fault. Branch of Schmidhausen-Inzenham-Zaissberg Fault [DE-BY_735].
SW-NE streichende Zweigstörung zur Schmidhausen-Inzenham-Zaissberg Störung [DE-BY_735]; ca. 70° nach NW einfallende antithetische Abschiebung.
Weitnau-Burggen Train of Faults
Weitnau-Burggen Störungszug
WSW-ENE trending, at Kempten veering to W-E, chain of approx. 75° to 85° SSE to S dipping synthetic normal faults.
WSW-ENE verlaufender, bei Kempten auf W-E drehender, ca. 75° bis 85° nach SSE bis S einfallender Störungszug synthetischer Abschiebungen.
Wertach-Stötten Fault
Wertach-Stötten Störung
W-E trending, approx. 75° S dipping synthetic normal fault south of Markt Oberdorf. In its eastern part, most likely linked via a relay ramp to Wald-Burggen Fault [DE-BY_1179] running subparallel to the south.
W-E verlaufende, ca. 75° nach S einfallende synthetische Abschiebung südlich von Markt Oberdorf. Im östlichen Teil höchstwahrscheinlich über eine Relay Ramp mit der südlich subparallel verlaufenden Wald-Burggen Fault [DE-BY_1179] verbunden.
Weitnau-Wertach Fault
Weitnau-Wertach Störung
Slightly undulating, overall WSW-ENE trending, approx. 80-85° SSE dipping synthetic normal fault; interconnection beneath Kempten inferred.
Leicht gewellt, insgesamt WSW-ENE verlaufende, ca. 80-85° nach SSE einfallende synthetische Abschiebung; Verbindung unter Kempten ist nicht gesichert.
Wald-Burggen Fault
Wald-Burggen Störung
WSW-ENE trending, approx. 75° SSE dipping synthetic normal fault. In its westernmost part, most likely connected via a relay ramp to Wertach-Stötten Fault [DE-BY_1178] running subparallel to the north.
WSW-ENE verlaufende, ca. 75° nach SSE einfallende synthetische Abschiebung. Im westlichsten Teil höchstwahrscheinlich über eine Relay Ramp mit der nördlich subparallel verlaufenden Wertach-Stötten Störung [DE-BY_1178] verbunden.
SW-NE trending, approx. 75° SE dipping normal fault
Sentenharter Verwerfung
Sentenharter Fault
SW-NE striking, approx. 55° NW dipping normal fault
SW-NE streichende, ca. 55° nach NW einfallende Abschiebung.
N-S streichende, ca. 85° nach W einfallende Abschiebung.
N-S trending, approx. 85° W dipping normal fault
WSW-ENE striking, approx. 75° SSE dipping normal fault
WNW-ESE streichende, ca. 75° nach SSE einfallende Abschiebung.
Grünwald Graben Fault System
Grünwalder Grabenbruch System
Subparallel array of WSW-ENE trending normal faults between Lake Starnberg and Oberhaching forming the eastern and western Grünwald Graben. The graben structure is target of the Oberhaching / Grünwald geothermal exploration and production drillings.
Subparallele Abfolge WSW-ENE verlaufender Abschiebungen zwischen dem Starnberger See und Oberhaching die den westlichen und östlichen Grünwald Graben bilden. Die Grabenstruktur ist Ziel der Oberhaching/Grünwald Geothermie-Erkundungs- und Erschließungsbohrungen.
Berg-Strasslach Fault
Berg-Straßlach Störung
WSW-ENE, approx. 55° SSE dipping synthetic normal fault.
WSW-ENE streichende, ca. 55° nach SSE einfallende synthetische Abschiebung.
Grünwalder Forst Fault
Grünwalder Forst Störung
Grünwald Störung
Undulate WSW-ENE trending, 80° SSE dipping synthetic normal fault featuring a throw up to 200 m. Northern boundary of eastern Grünwald Graben.
Gewellt WSW-ENE verlaufende, ca. 80° nach SSE einfallende synthetische Abschiebung mit einem Vertikalveratz bis zu 200 m; Nordflanke des östlichen Grünwald Grabens.
Strasslach-Oberhaching Fault
Straßlach-Oberhaching Störung
Slightly undulate WSW-ENE trending, approx. 70° NNW dipping antithetic normal fault featuring a throw of about 80 m. Southern boundary of western and eastern Grünwald Graben.
Leicht gewellt WSW-ENE verlaufende, ca. 70° nach NNW einfallende antithetische Abschiebung mit einer Sprunghöhe von rund 80 m. Südflanke des westlichen und östlichen Grünwald Grabens.
Kempfenhausen Fault
Kempfenhausen Störung
SW-NE striking, approx. 80° NW dipping antithetic normal fault.
SW-NE streichende, ca. 80° nach NW einfallende antithetische Abschiebung.
WSW-ENE trending, approx. 80° NNW dipping antithetic normal fault with a minor throw running within eastern Grünwald Graben.
Im östlichen Grünwald Graben WSW-ENE verlaufende, ca. 80° nach NNW einfallende antithetische Abschiebung mit geringem Vertikalversatz.
Oberhaching Fault
Oberhaching Störung
Schorn-Grünwald Fault
Schorn-Grünwald Störung
SW-NE to E-W trending, approx. 70° SE to S dipping synthetic normal fault.
SW-NE bis E-W verlaufende, ca. 70° nach SE bis S einfallende synthetische Abschiebung.
Altmühldorf-Tüssling Fault
Altmühldorf-Tüßling Störung
Slightly northeastward arcuate overall NW-SE trending, approx. 65° ± NE dipping antithetic normal fault. In parts inferred segment of the southwestern boundary of Gifthal Trough, a northwestward widening graben-like structure along the southwestern scarp of Landshut-Neuötting crystalline rise. The apparent segmentation of this borderline, emerging from proved Taufkirchen-Ampfing Fault [DE-BY_793], arguably results from subseismic throws related to flexure-like segments, the incremental onlap of the Gifthal Trough onto the lower step of Landshut-Neuötting rise confined by Fault Scarp 3 [DE-BY_703], and the overthrust caused by Grasset-Wechselberg reverse fault [DE-BY_1224].
Leicht nach NE gebogen, insgesamt NW-SW verlaufende, ca. 65° nach NE einfallende antithetische Abschiebung. Südwestliche Grenze des Gifthal Trogs, einer sich nach NW hin aufweitenden Grabenstruktur entlang des südwestlichen Abbruchs des Landshut-Neuötting Hochs. Die augenscheinliche Segmentierung der Trogflanke, als Fortsetzung der seismisch nachgewiesenen Taufkirchen-Ampfing Störung [DE-BY_793], resultiert aus der abschnittsweisen „Unsichtbarkeit“ in seismischen Profilen, wahrscheinlich bedingt durch subseismische, flexurartige Abschnitte in Verbindung mit dem schleifenden Anstieg auf die unterste Staffel des Landshut-Neuötting Abbruchs, begrenzt von der Abbruchstufe 3 [DE-BY_703], sowie die Überfahrung durch die Grasset-Wechselberg Aufschiebung [DE-BY_1224].
Taufkirchen-Ampfing Fault
Taufkirchener Abbruch
Taufkirchen-Ampfing Störung
From WSW-ENE to NW-SE veering, averaged approx. 60° NNW to NE dipping antithetic normal fault. Likewise the close-by Velden Fault [DE-BY_711], this fault north of Dorfen veers from the "Central Molasse Basin" characteristic strike to the "Lower Bavaria Molasse Basin" characteristic trend when approaching the Landshut-Neuötting crystalline rise. Continuing as Altmühldorf-Tüssling Fault [DE-BY_1221] along the southwestern flank of Gifthal Trough, finally vanishing at the onlap of Gifthal Trough onto the stepped flank of Landshut-Neuötting crystalline rise [DE-BY_700].
Von WSW-ENE auf NW-SE Verlauf drehend, im Mittel ca. 60° nach NNW bis NE einfallende antithetische Abschiebung nördlich von Dorfen. Gleich wie bei der nordöstlich gelegenen Velden Störung, folgt der Verlauf dieser Störung in ihrem westlichen Teil der für die zentrale Vorlandmolasse typischen Richtung und dreht mit Annäherung an das Landshut-Neuötting Hoch auf herzynische, für das Niederbayerische Molassebecken charakteristische Richtung und zieht sich als Altmühldorf-Tüßling Störung [DE-BY_1221], entlang der südwestlichen Flanke des Gifthal Trogs, der sich schleifend auf den Landshut-Neuötting Abbruch [DE-BY_700] zieht.
Isnerberg-Unterried Fault
Isnerberg-Unterried Störung
N-S striking, approx. 60° E dipping antithetic normal fault.
N-S streichende, ca. 60° nach E einfallenden antithetische Abschiebung.
NNW-SSE streichende, ca. 85° nach WSW einfallende Abschiebung.
NNW-SSE striking, approx. 85° WSW dipping normal fault
W-E streichende, ca. 65° nach S einfallende Abschiebung.
W-E striking, approx. 65° S dipping normal fault
Haindlfing-Erlau Fault
Haindlfing-Erlau Störung
W-E to WNW-ESE trending, approx. 75° N to NNE dipping antithetic normal fault north of Freising. Conjugate with synthetic Burghausen-Zolling Fault [DE-BY_827] it forms a wedge-shaped graben structure levelling out to the east.
W-E bis WNW-ESE verlaufende, ca. 75° nach N bis NNE einfallende antithetische Abschiebung nördlich von Freising. Bildet zusammen mit der synthetischen Burghausen-Zolling Störung [DE-BY_827] eine keilförmige, nach Osten auslaufende Grabenstruktur.
Thalhausen Fault
Thalhausen Störung
WSW-ENE striking, approx. 85° SSE dipping synthetic normal fault NW of Freising.
WSW-ENE streichende, ca. 85° nach SSE einfallende synthetische Abschiebung NW von Freising.
Giggenhausen Fault
Giggenhausen Störung
W-E trending, approx. 65° S dipping synthetic normal fault SW of Freising
W-E verlaufende, ca. 65° nach S einfallende synthetische Abschiebung SW von Freising.
Burghausen-Zolling Fault
Burghausen-Zolling Störung
WSW-ENE trending, approx. 80° SSE dipping synthetic normal fault north of Freising.
WSW-ENE verlaufende, ca. 80° nach SSE einfallende synthetische Abschiebung nördlich von Freising.
Grossnöbach-Pulling Fault
Großnöbach-Pulling Störung
Slightly undulated overall W-E trending, approx. 65° ± S dipping synthetic normal fault southwest of Freising.
Leicht wellenförmig W-E verlaufende, ca. 65° nach ± S einfallende synthetische Abschiebung südwestlich von Freising.
Nesselwang-Steingaden Fault System
Nesselwang-Steingaden Störungssystem
WSW-ENE trending array of steeply dipping normal faults underneath the Subalpine Molasse. The faults of this array in sections are forming local graben structures with the northward subparallel Rückholz Fault [DE-BY_841].
WSW-ENE verlaufende Gruppe steil einfallender Abschiebungen unter der Faltenmolasse. Südlich subparallel zur Rückholz Störung [DE-BY_841], mit der die Teilstörungen abschnittsweise lokale Grabenstrukturen bilden.
Rosshaupten-Prem Fault
Roßhaupten-Prem Störung
WSW-ENE striking, approx. 85° SSE dipping synthetic normal fault
Lechbruck Fault
Lechbruck Störung
Seeg-Steingaden Fault
Seeg-Steingaden Störung
Undulate WSW-ENE trending, approx. 65° NNW dipping antithetic normal fault.
Gewellt WSW-ENE verlaufende, ca. 65° nach NNW einfallende antithetische Abschiebung.
Seeg Fault
Seeg Störung
WSW-ENE striking, approx. 75° SSE dipping synthetic normal fault
WSW-ENE streichende, ca. 75° nach SSE einfallende synthetische Abschiebung
Maria Rain Fault
Maria Rain Störung
WSW-ENE striking, approx. 75° NNE dipping antithetic normal fault.
WSW-ENE streichende, ca. 75° nach NNE einfallende antithetische Abschiebung.
Rückholz Fault
Rückholz Störung
W-E to WSW-ENE trending, approx. 65° S to SSE dipping synthetic normal fault.
W-E bis WSW-ENE verlaufende, ca. 65° nach S bis SSE einfallende synthetische Abschiebung.
Waltenhofen-Görisried Faults
Waltenhofen-Görisried Störungen
Group of WSW-ENE to WNW-ESE striking, steeply (85°-60°) dipping syn- and antithetic normal faults southwest of Kempten, in between Weitnau-Wertach Fault [DE-BY_1177] to the north and Oberreute-Oy-Mittelberg Fault [DE-BY_832] to the south.
Gruppe WSW-ENE bis WNW-ESE streichender, steil (85°-60°) einfallender syn- und antithetischer Abschiebungen SW von Kempten zwischen der Weitnau-Wertach Störung [DE-BY_1177] im Norden und der Oberreute-Oy-Mittelberg Störung [DE-BY_832] im Süden.
Oberreute-Oy-Mittelberg Fault
Oberreute-Oy-Mittelberg Störung
Overall WSW-ENE trending, on average, approx. 75° SSE dipping synthetic normal fault, linked to Rückholz Fault [DE-BY_841] in the east.
Insgesamt WSW-ENE streichende, durchschnittlich ca. 75° nach SSE einfallende synthetische Abschiebung die sich im Osten in der Rückholz Störung [DE-BY_841] fortsetzt.
Kirchdorf-Thonhausen Fault
Kirchdorf-Thonhausen Störung
W-E to WSW-ENE trending, approx. 65° S to SSE dipping synthetic normal fault north of Freising.
W-E bis WSW-ENE verlaufende, ca. 65° nach S bis SSE einfallende synthetische Abschiebung nördlich von Freising.
SW-NE striking, approx. 65° NW dipping normal fault/fault zone, downthrow of SE-block about 40 m.
Schwackenreuter Störungszone
Schwackenreut Main Fault
SW-NE streichende, ca. 65° nach NW einfallende Abschiebung, NW-Teil etwa 40 m abgesunken
Nebenstörung Schwackenreuter Verwerfung
Schwackenreut Subfault
Saulgau Main Fault
Saulgauer Hauptverwerfung
WSW-ENE bis SW-NE streichende, ca. 70° nach NNW bis NW einfallende Störungszone, NW-Teil abgesunken, max. 200 m vertikaler Versatzbetrag
WSW-ENE to SW-NE trending, approx 70° NNW to NW dipping normal fault system, downthrow of NW-part max 200 m
[hl_010_b]
Störungszone Bad Waldsee
NE-SW trending fault zone, downthrow of SE-block max. 25 m.
NE-SW streichende Störungszone, SE-Scholle max. 25 m abgesunken.
Bad Waldsee Fault Zone
SSW-NNE streichende, ca. 60° nach ESE einfallende Abschiebung.
SSW-NNE striking, approx. 60° ESE dipping normal fault.
NNW-SSE streichende, ca. 70° nach ENE einfallende Abschiebung.
NNW-SSE striking, approx. 70° ENE dipping normal fault.
[lca_054]
NW-SE streichende, ca. 50° nach NE einfallende Abschiebung.
NW-SE striking, approx. 50° NE dipping normal fault.
WSW-ENE striking, approx. 55° SSE dipping normal fault.
WSW-ENE streichende, ca. 55° nach SSE einfallende Abschiebung.
[lca_006_a]
[lca_006_b]
WSW-ENE trending, approx. 80° SSE dipping normal fault.
Traunreut Step Fault
Traunreut Bruchstaffel
Structure located nearby oil- and gasfield Traunreut. Staggered array of roughly W-E trending ± 60° S dipping synthetic normal faults.
Am Öl- und Gasfeld Traunreut gelegene, ungefähr W-E verlaufende Bruchstaffel von ± 60° nach S einfallenden synthetischen Abschiebungen.
Hörpolding Fault
Hörpolding Störung
WSW-ENE striking, approx. 60° SSE dipping fault scarp of the Traunreut Step Fault.
WSW-ENE streichende, ca. 60° nach SSE einfallende Bruchstufe der Traunreut Bruchstaffel.
Truchtlaching-Traunreut Fault
Truchtlaching-Traunreut Störung
W-E to WSW-ENE striking, approx. 60° S to SSE dipping fault scarp of the Traunreut Step Fault.
W-E bis WSW-ENE streichende, ca. 60° südfallende Bruchstufe der Traunreut Bruchstaffel.
Seeon-Traunreut Fault
Seeon-Traunreut Störung
W-E striking, approx. 60° S dipping fault scarp of the Traunreut Step Fault.
W-E streichende, ca. 60° südfallende Bruchstufe der Traunreut Bruchstaffel.
Störungszone Ilmensee-Fronhofen-Aulendorf
Ilmensee-Fronhofen-Aulendorf Fault Zone
SW-NE streichende Störungszone, NW-Teil abgesunken, max. 100 m vertikaler Versatzbetrag.
SW-NE trending fault zone, downthrown of NW-block max. 100 m
SW-NE striking, approx. 70° NW dipping normal fault. Northern boundary of Frohnhofen-Illensee oil and gas fields.
SW-NE streichende, ca. 70° nach NW einfallende Abschiebung. Nordgrenze der Öl- und Gasfelder Frohnhofen-Illmensee.
[lca_065]
[hl_097_b]
[lca_008]
WSW-ENE trending, approx. 65° NNW dipping normal fault.
WSW-ENE streichende, ca. 65° nach NNW einfallende Abschiebung.
WSW-ENE streichende, ca. 75° nach SSE einfallende Abschiebung.
Innthal-Mauerkirchen Fault
Innthal-Mauerkirchen Störung
W-E striking, approx. 70° S dipping synthetic normal fault south of Bad Endorf.
W-E streichende, ca. 70° nach S einfallende synthetische Abschiebung südlich von Bad Endorf.
Flaches SE-NW verlaufendes Grabensystem.
Eichberg-Kirchdorf a.d. Iller Fault Zone
Störungszone Eichberg-Kirchdorf a.d. Iller
Shallow SE-NW trending graben system.
Bad Endorf Fault
Bad Endorf Störung
W-E striking, approx. 80° S dipping synthetic normal fault.
Störungszone Ochsenhausen-Kirchberg a.d. Iller
NE-SW streichende Störungszone, NW-Teil max. 50 m abgesunken.
Ochsenhausen-Kirchberg a.d. Iller Fault Zone
NE-SW trending fault zone, downthrown of NW-part max. 50 m.
N-S striking, approx. 70° W dipping normal fault.
N-S streichende, ca. 70° nach W einfallende Abschiebung.
N-S streichende, ca. 80° nach W einfallende Abschiebung.
N-S striking, approx. 80° W dipping normal fault.
Almertsham Fault
Almertsham Störung
Structure located nearby oil- and gasfield Almertsham. Slightly northward arcuate W-E trending, approx. 60° N dipping antithetic normal fault north of Bad Endorf.
Am Öl- und Gasfeld Almertsham gelegene, leicht nordwärts gebogene, W-E verlaufende, ca. 60° nach N einfallende antithetische Abschiebung nördlich von Bad Endorf.
Störungszone Mönchsrot-Ellwangen (Ellbach)
Mönchsrot-Ellwangen (Ellbach) Fault Zone
SW-NE streichende Störungszone, NW -Scholle etwa 50 m abgesunken.
SW-NE trending fault zone, downthrow of NW-block about 50 m.
Slightly undulate SW-NE striking, approx. 65° NW dipping normal fault.
Leicht gewellt SW-NE verlaufende, ca. 65° nach NW einfallende Abschiebung.
Gewellt WSW-ENE verlaufende, ca. 65° nach NNW einfallende Abschiebung, Seitenast von [DE-BW_176].
Undulate WSW-ENE trending, approx. 65° NNW dipping normal fault, branch of [hl_114].
W-E streichende, ca. 65° nach N einfallende Abschiebung, Seitenast von [DE-BW_177].
W-E striking, approx. 65° N dipping normal fault, branch of [hl_131].
WNW-ESE striking, approx. 55° NNE dipping normal fault, lateral fault connecting [hl_108] and [hl_129].
WNW-ESE streichende, ca. 55° nach NNE einfallende Abschiebung, Querstörung zwischen [DE-BW_033] und [DE-BW_179].
Arcuate WSW-ENE trending, approx. 85° SSE dipping normal fault, in its NE closely subparallel to [hl_128].
Gebogen WSW-ENE verlaufende, ca. 85° nach SSE einfallende Abschiebung, im NE subparallel zur nahen [DE-BW_188].
[lca_052]
[hl_108_b]
Arcuate SW-NE trending, approx. 75° NW dipping normal fault, link between [hl_108] and [hl_125].
Gebogen SW-NE verlaufende, ca. 75° nach NW einfallende Abschiebung, Verbindung zwischen [DE-BW_033] and [DE-BW_189].
Undulate SW-NE trending, approx. 75° NW dipping normal fault closely subparallel to [hl_126].
Gewellt SW-NE verlaufende, ca. 75° nach NW einfallende Abschiebung subparallel zur nahen [DE-BW_186].
Branching off [hl_126], undulate W-E trending, approx. 65° ± S dipping normal fault.
Abzweig von [hl_126], gewellt W-E verlaufende, ca. 65° nach ± S einfallende Abschiebung.
SW-NE streichende, ca. 55° nach SE einfallende Abschiebung.
[lca_051]
SW-NE striking, approx. 55° SE dipping normal fault.
SSW-NNE striking, approx. 45° ESE dipping normal fault.
SSW-NNE streichende, ca. 45° nach ESE einfallende Abschiebung.
[lca_049]
Rast Fault
Rast Verwerfung
SSW-NNE trending, approx. 65° WNW dipping normal fault
Krumbach Fault
SW-NE striking, approx. 65° NW dipping normal fault/fault zone, downthrow of NW block max. 140 m.
SW-NE streichende Störungszone, NW -Teil abgesunken, max. 140 m Versatzbetrag
Krumbacher Verwerfung
Assing-Bromberg Fault System
Assing-Bromberg Störungssystem
Northern boundary of oil- and gasfields Assing and Bromberg. WNW-ESE trending 70°-80° NNE dipping antithetic normal faults running from Palling towards Laufen/Inn.
Nördliche Begrenzung der Öl- und Gasfelder Assing und Bromberg. WNW-ESE von Palling Richtung Laufen/Inn verlaufende, 70°-80° nach NNE einfallende antithetische Abschiebungen.
Tettenhausen-Kirchanschöring Fault
Tettenhausen-Kirchanschöring Störung
WNW-ESE striking, approx. 75° NNE dipping antithetic normal fault.
WNW-ESE verlaufende, ca. 75° nach NNW einfallende antithetische Abschiebung.
Gessenhausen-Thannsberg Fault
Gessenhausen-Thannsberg Störung
Palling-Mauerham Fault
Palling-Mauerham Störung
WNW-ESE striking, approx. 80° NNE dipping antithetic normal fault.
WNW-ESE verlaufende, ca. 80° nach NNW einfallende antithetische Abschiebung.
Strassbach-Vierkirchen Fault
Straßbach-Vierkirchen Störung
SW-NE striking, approx. 75° NW dipping antithetic normal fault.
SW-NE streichende, ca. 75° nach NW einfallende antithetische Abschiebung.
Vierkirchen-Leonhardsbuch Fault
Vierkirchen-Leonhardsbuch Störung
SW-NE striking, approx. 55° SE dipping synthetic normal fault.
SW-NE streichende, ca. 55° nach SE einfallende synthetische Abschiebung.
Petershausen-Schweitenkirchen Fault
Petershausen-Schweitenkirchen Störung
SW-NE striking, approx. 75° SE dipping synthetic normal fault.
SW-NE streichende, ca. 75° nach SE einfallende synthetische Abschiebung.
Ilmmünster Step Fault
Ilmmünster Bruchstaffel
Staggered array of 5 (sub-)parallel W-E to SW-NE striking, steeply (85°-60°) S to SSE dipping synthetic normal faults scarps with minor throws immediate south of Pfaffenhofen Step Fault [DE-BY_767]. Beyond the five detected faults featuring throws of more than about 10 m, more subseismic fault scarps are possible.
Bruchstaffel aus fünf (sub)parallelen, W-E bis SW-NE verlaufenden, steil (85°-60°) nach S bis SSE einfallenden synthetischen Abschiebungen mit geringer Sprunghöhe, unmittelbar südlich der antithetischen Pfaffenhofen Bruchstaffel [DE-BY_767]. Neben den fünf identifizierbaren Stufen mit Sprunghöhen von mehr als ca. 10 m sind weitere subseismische Bruchstufen möglich.
N-S striking normal fault dipping W with unknown angle.
Weiherholz Verwerfung
Weiherholz Fault
Velden Fault
Velden Störung
From WSW-ENE strike veering to NW-SE trend, averaged approx. 55° NNW to NE dipping antithetic normal fault; northern boundary of oil- and gasfield Velden. This fault runs within the Gifthal Trough from Taufkirchen/Vils to Oberbergkirchen veering from the "Central Molasse Basin" characteristic trend to the "Lower Bavaria Molasse Basin" typical strike when approaching the Landshut-Neuötting crystalline rise and ends, forking into proven horsetail splays, ESE of Oberbergkirchen.
Von Taufkirchen/Vils bis Oberbergkirchen, von WSW-ENE auf NW-SE drehend verlaufende, im Mittel ca. 55° nach NNW bis NE einfallende antithetische Abschiebung; nördliche Begrenzung der Öl- und Gasfelds Velden. Der Verlauf der Störung folgt dem Gifthal Trog, im westlichen Teil in für die zentrale Vorlandmolasse typischer Richtung, dreht mit Annäherung an das Landshut-Neuötting Hoch auf herzynische, für das Niederbayerische Molassebecken charakteristische Richtung und fiedert ESE von Oberbergkirchen in kleine, zunehmend subseismische Störungsäste (horsetail splay) auf.
Seebruck Fault
Seebruck Störung
W-E striking, approx. 65° S dipping synthetic normal fault at the northern shore of Chiemsee.
W-E streichende ca. 65° nach S einfallende synthetische Abschiebung am Nordufer des Chiemsee.
Höslwang Fault
Höslwang Störung
W-E striking, approx. 70° S dipping synthetic normal fault running from Halfing to Eschenauer See.
W-E streichende, ca. 70° nach S einfallende synthetische Abschiebung zwischen Halfing und Eschenauer See.
Stetten-Arzbach Fault
Stetten-Arzbach Störung
SW-NE striking, approx. 60° SE dipping synthetic normal fault NW of Dachau.
SW-NE streichende, ca. 55° nach 60 einfallende synthetische Abschiebung NW von Dachau.
Arzbach-Fahrenzhausen Fault
Arzbach-Fahrenzhausen Störung
SW-NE striking, approx. 80° NW dipping antithetic normal fault north of Dachau.
SW-NE streichende, ca. 80° nach NW einfallende antithetische Abschiebung nördlich von Dachau.
Biberbach-Bachhausen Fault
Biberbach-Bachhausen Störung
SSW-NNE trending, approx. 85° WNW dipping normal fault
WSW-ENE striking, approx. 80° NNW dipping normal fault
WSW-ENE streichende, ca. 80° nach NNW einfallende Abschiebung.
Höhenrain Fault
Höhenrain Störung
Northern boundary of oil- and gasfield Höhenrain. Undulate SW-NE to W-E trending, approx. 70° NW to N dipping antithetic normal fault running from Holzkirchen to Rott am Inn.
Nördliche Begrenzung des Öl- und Gasfeldes Höhenrain. Von Holzkirchen bis Rott am Inn gewellt SW-NE bis W-E verlaufende, ca. 70° nach NW bis N einfallende antithetische Abschiebung.
Dachau-Inhausen Fault
Dachau-Inhausen Störung
SW-NE striking, approx. 60° SE dipping synthetic normal fault.
SW-NE streichende, ca. 60° nach SE einfallende synthetische Abschiebung.
Gars-Garching Fault
Gars-Garching Störung
W-E trending, approx. 75° S dipping synthetic normal fault running from S of Gars/Inn to N of Garching/Alz.
W-E verlaufende, ca. 75° nach S einfallende synthetische Abschiebung zwischen S von Gars am Inn und N von Garching an der Alz.
Dachau-Unterschleissheim Fault
Dachau-Unterschleißheim Störung
SW-NE striking, >85° SE dipping synthetic normal fault.
SW-NE streichende, >85° nach SE einfallende synthetische Abschiebung.
Bierwang Fault
Bierwang Störung
Nördliche Begrenzung des Öl- und Gasfeldes Bierwang. WSW-ENE verlaufende, ca. 50° nach NNW einfallende antithetische Abschiebung zwischen Soyen und Taufkirchen.
Northern boundary of oil- and gasfield Bierwang. WSW-ENE trending, approx. 50° NNW dipping dipping antithetic normal fault running from Soyen to Taufkirchen.
Albaching-Rechtmehring Fault
Albaching-Rechtmehring Störung
Northern boundary of oil- and gasfields Albaching and Rechtmehring. WSW-ENE to W-E trending, on average approx. 75° NNW to N dipping antithetic normal fault running from Kirchseeon to the Inn river SE of Haag. At its western end possibly conected to Wächterhof-Kirchseeon Fault [DE-BY_1094] via a relay ramp.
WSW-ENE bis W-E verlaufende, im Mittel ca. 75° nach NNW bis N einfallende antithetische Abschiebung zwischen Kirchseeon und dem Inn SE von Haag. Nördliche Begrenzung der Öl- und Gasfelder Albaching und Rechtmehring. Am östlichen Ende möglicherweise über eine Relais Rampe (relay ramp) mit der Wächterhof-Kirchseeon Störung [DE-BY_1094] verbunden.
Einsbach-Dachau Fault
Einsbach-Dachau Störung
Undulate W-E trending, approx. 60° S dipping synthetic normal fault.
Gewellt W-E verlaufende, ca. 60° nach S einfallende synthetische Abschiebung.
Dachau Subfault
Dachau Nebenstörung
W-E trending, approx. 50° S dipping synthetic normal fault.
W-E verlaufende, ca. 50° nach S einfallende synthetische Abschiebung.
Wächterhof-Kirchseeon Fault
Wächterhof-Kirchseeon Störung
WSW-ENE to W-E trending, approx. 70° NNW to N dipping antithetic normal fault. At its eastern end possibly connected to Albaching-Rechtmehring Fault [DE-BY_723] via a relay ramp.
WSW-ENE bis W-E verlaufende, ca. 70° nach NNW bis N einfallende antithetische Abschiebung. Am östlichen Ende möglicherweise über eine Relais Rampe (relay ramp) mit der Albaching-Rechtmehring Fault [DE-BY_723] verbunden.
Fuchstal Fault
Fuchstal Störung
SW-NE striking, approx. 70° SE dipping synthetic normal fault.
SW-NE streichende, ca. 70° nach SE einfallende synthetische Abschiebung.
Anzing-Ödgassen-Waldkraiburg Fault
Anzing-Ödgassen-Waldkraiburg Störung
Running from Anzing E of Munich to Polling S of Mühldorf, undulate WSW-ENE trending, on average approx. 55° NNW dipping antithetic normal fault; northern boundary of oil- and gasfields Anzing, Schnaupping, Haag, Ödgassen, Waldkraiburg, and Mühldorf-Süd.
Wellenförmig WSW-ENE verlaufende im Mittel ca. 55° nach NNW einfallende antithetische Abschiebung zwischen Anzing und Polling S von Mühldorf. Nördliche Begrenzung der Öl- und Gasfelder Anzing, Schnaupping, Haag und Ödgassen, Waldkraiburg und Mühldorf-Süd.
Hagenheim-Finning Fault
Hagenheim-Finning Störung
SW-NE striking, approx. 85° SE dipping synthetic normal fault.
SW-NE streichende, ca. 85° nach SE einfallende synthetische Abschiebung.
Stiefenhofen-Weitnau Fault
Stiefenhofen-Weitnau Störung
WSW-ENE striking, approx. 60° SSE dipping synthetic normal fault.
WSW-ENE streichende, ca. 50° nach SSE einfallende Abschiebung.
[lca_070]
WSW-ENE striking, approx. 50° SSE dipping normal fault
[lca_071]
[lca_072]
[lca_073]
SSW-NNE striking, approx. 50° WNW dipping normal fault
SSW-NNE streichende, ca. 50° nach WNW einfallende Abschiebung.
Kinsau Fault
Kinsau Störung
Northern boundary of oilfield Kinsau. W-E trending, approx. 55° N dipping antithetic normal fault running from Kaltental to Reichling.
Nördliche Begrenzung des Öl-Feldes Kinsau. W-E verlaufende, ca. 55° nach N einfallende antithetische Abschiebung zwischen Kaltental und Reichling.
Günzach-Pforzen Fault
Günzach-Pforzen Störung
SW-NE striking, approx. 70° NW dipping antithetic normal fault.
SW-NE streichende, ca. 70° nach NW einfallende antithetische Abschiebung.
Freising Fault
Freising Störung
Slightly undulated overall W-E trending, approx. 55° ± N dipping antithetic normal fault running from Kranzberg to Schmidhausen.
Leicht wellenförmig W-E verlaufende, ca. 55° nach ± N einfallende antithetische Abschiebung zwischen Kranzberg und Schmidhausen.
Utrasried-Irsee Fault
Utrasried-Irsee Störung
Slightly undulating SW-NE to SSW-NNE trending, approx. 50° SE to ESE dipping synthetic normal fault.
Leicht gewellt SW-NE bis SSW-NNE verlaufende, ca. 50° nach SE bis ESE einfallende synthetische Abschiebung.
Grossnöbach-Massenhausen Fault
Großnöbach-Massenhausen Störung
W-E striking, approx. 85° N dipping antithetic normal fault.
W-E streichende, ca. 85° N einfallende antithetische Abschiebung.
Blöcktach-Bad Wörishofen Fault
Blöcktach-Bad Wörishofen Störung
SSW-NNE striking, approx. 80° WNW dipping antithetic normal fault.
SSW-NNE streichende, ca. 80° nach WNW einfallende antithetische Abschiebung.
Dachau-Grossnöbach Fault
Dachau-Großnöbach Störung
Arcuate SW-NE to SSW-NNE trending, approx. 75° ± SE dipping synthetic normal fault.
Bogenförmig SW-NE bis SSW-NNE verlaufende, ca. 75° nach ± SE einfallende synthetische Abschiebung.
[lca_078]
[lca_079]
[lca_074]
[lca_075]
[lca_076]
Mauerstetten-Markt Schwaben Train of Faults
Mauerstetten-Markt Schwaben Störungszug
Chain of major synthetic normal faults running from Kempten to Markt Schwaben.
Lineare Anordnung größerer synthetischer Abschiebungen zwischen Kempten und Markt Schwaben.
Rott Linking Faults
Rott Störungsschar
En Echelon step fault like cluster of subparallel, overall SW-NE trending, steeply (85°-60°) ± SE dipping synthetic normal faults at the transition from Mauerstetten Step Fault [DE-BY_755] to Munich Fault [DE-BY_1100].
Bruchstaffel subparalleler, insgesamt SW-NE verlaufender, steil (85°-60°) nach ± SE einfallender synthetischer Abschiebungen am Übergang des Mauerstetten Abbruchs [DE-BY_755] zum Münchener Verwurf [DE-BY_1100].
Mauerstetten Step Fault
Mauerstetten Störung
Mauerstetten Abbruch
Overall WSW-ENE oriented step fault system of up to 4 steeply (55°-85°) ± SSE dipping normal fault scarps.
Übergeordnet WSW-ENE verlaufendes System von bis zu 4 Abbruchstufen aus steilstehenden (55°-85°) Abschiebung mit ± SSE-Einfallen.
Mauerstetten Fault Scarp 4
Mauerstetten Abbruchstufe 4
Mauerstetten Step Fault far southeastern scarp running from Markt Oberdorf to Osterzell. SSW-NNE trending, approx. 85° ESE dipping synthetic normal fault.
Südöstlichste Bruchstufe des Mauerstetten Abbruchs zwischen Markt Oberdorf und Osterzell. SSW-NNE verlaufende, ca. 85° nach ESE einfallende synthetische Abschiebung.
Mauerstetten Fault Scarp 3
Mauerstetten Abbruchstufe 3
Mauerstetten Step Fault southeastern scarp running from Aitrang to Stöttwang. WSW-ENE to SW-NE trending, approx. 60° ± SE dipping synthetic normal fault.
Südöstliche Bruchstufe des Mauerstetten Abbruchs zwischen Aitrang und Stöttwang. WSW-ENE bis SW-NE verlaufende, ca. 60° nach ± SE einfallende synthetische Abschiebung.
Mauerstetten Fault Scarp 2
Mauerstetten Abbruchstufe 2
Mauerstetten Step Fault main scarp running from north of Kempten to Mauerstetten and eastbound on towards the Lech river. WSW-ENE to W-E trending, approx. 55° SSE to S dipping synthetic normal fault.
Mittlere Bruchstufe des Mauerstetten Abbruchs von nördlich Kempten über Mauerstetten ostwärts bis nach Dienhausen. WSW-ENE bis W-E verlaufende, ca. 55° nach SSE bis S einfallende synthetische Abschiebung.
Mauerstetten Fault Scarp 1
Mauerstetten Abbruchstufe 1
Mauerstetten Step Fault northwestern scarp running from Günzach to Mauerstetten. Southwestward arcuate WSW-ENE trending, approx. 65° SSE dipping synthetic normal fault.
Nordwestliche Bruchstufe des Mauerstetten Abbruchs zwischen Günzach und Mauerstetten. Südwestwärts gebogen WSW-ENE verlaufende, ca. 65° nach SSE einfallende synthetische Abschiebung.
Apfeldorf Fault
Apfeldorf Störung
WSW-ENE striking, approx. 85° SSE dipping synthetic normal fault at the transition from Mauerstetten Step Fault [DE-BY_755] to Munich Fault [DE-BY_1100].
WSW-ENE streichende, ca. 85° nach SSE einfallende synthetische Abschiebung am Übergang des Mauerstetten Abbruchs [DE-BY_755] zum Münchener Verwurf [DE-BY_1100].
Markt Schwaben Fault
Markt Schwaben Verwurf
Markt Schwabener Verwurf
Emerging from the horsetail splay at the eastern end of Munich Fault [DE-BY_1100], this WSW-ENE trending major structure featuring a throw up to 200 m (Dussel et al. 2015) consists of two approx. 75° SSE dipping synthetic normal faults, soft-linked by a relay ramp. Principal target of several deep E&P drillings for hydrothermal heat production.
Östliche Fortsetzung des Münchener Verwurfs [DE-BY_1100]. WSW-ENE verlaufende Struktur, bestehend aus zwei ca. 75° nach SSE einfallenden synthetischen Abschiebungen mit einem Versatz bis zu 200 m (Dussel et al. 2015), die über eine Relais Rampe (relay ramp) miteinander in Verbindung stehen. Zielstruktur hydrothermaler Förderbohrungen zur Wärmegewinnung.
Munich Fault
Münchener Verwurf
Overall WSW-ENE trending, on average approx. 70° SSE dipping synthetic normal fault running from west of Lake Ammer (Ammersee) to the eastern districts of Munich. Principal long-range fault of the Molasse Basin featuring a throw up to 350 m in the Munich area where forkings into several horsetail splays are proven.
Von Rott westlich des Ammersees bis zu den östlichen Stadteilen Münchens, insgesamt WSW-ENE verlaufende, im Mittel ca. 70° nach SSE einfallende synthetische Abschiebung. Eine der Hauptstörungen des Molassebeckens mit Versätzen bis zu 350 m im Raum München, wo eine mehrfache Auffiederung (horsetail splays) seismisch nachgewiesen ist.
WNW-ESE streichende, ca. 60° nach NNE einfallende Abschiebung.
WNW-ESE striking, approx. 60° NNE dipping normal fault
[lca_083]
[lca_084]
Darching Fault
Darching Störung
Northern boundary of oil- and gasfield Darching / Holzkirchen. Slightly undulate WNW-ESE trending, approx. 75° NNE dipping antithetic normal fault running from Holzkichen to Götting.
Nördliche Begrenzung des Öl- und Gasfeldes Darching / Holzkirchen. Leicht gewellt WNW-ESE verlaufende, ca. 75° nach NNE einfallende antithetische Abschiebung zwischen Holzkirchen und Götting.
Holzkirchen Fault
Holzkirchen Störung
NW-SE striking, approx. 80° NE dipping antithetic branch of Darching Fault.
NW-SE streichender, ca. 80° antithetisch nach NE einfallender Zweig der Darching Störung.
[lca_080]
[lca_089]
[lca_088]
N-S striking, approx. 85° W dipping normal fault
Frauenzell-Böhen Fault
Frauenzell-Böhen Störung
SW-NE trending, approx. 70° SE dipping synthetic normal fault.
SW-NE verlaufende, in etwa 70° nach SE einfallende synthetische Abschiebung.
Berg-Poing Train of Faults
Berg-Poing Störungszug
Train of synthetic faults running from Lake Starnberg to Poing east of Munich, partly linked through horsetail splay structures and an inferred (subseismic) relay ramp. Target of several successful geothermal exploitations and featuring some of the most prolific geothermal installations in the Greater Munich Area.
Vom Starnberger See bis Poing östlich von München reichender Störungszug teilweise über Auffiederungen (horsetail splay) und eine vermutete, subseismische Relais Rampe (relay ramp) verbundener Syntheter. Zielstruktur verschiedener erfolgreicher Tiefengeothermie Erschließungsvorhaben im Großraum München.
SW-NE striking, approx. 75° SE dipping synthetic normal fault, at its southwestern end presumably soft-linked to Taufkirchen-Parsdorf Fault [DE-BY_1085] via a relay ramp.
SW-NE streichende, ca. 75° nach SE einfallende synthetische Abschiebung. Am südwestlichen Ende vermutlich über eine Relais Rampe (relay ramp) mit der Taufkirchen-Parsdorf Störung [DE-BY_1085] verbunden.
Poing Fault
Poing Störung
Unterhaching Fault System
Unterhachinger Störungssystem
Northeastward forking structure consisting of three main faults, in sections split up into or dwindling in horsetail splay structures, forming a northwestern elevated ramp (horst) and a southeastern graben structure. The complex fault network of Unterhaching Faultsystem represents the target structure of several successful geothermal exploitations, featuring some of the most prolific deep geothermal installations in the Greater Munich Area.
Nach NE hin sich erweiternde und auslaufende Struktur aus drei, bereichsweise in mehrere Äste aufgefiederter Hauptstörungen. Die Störungen begrenzen einen rampenartigen Horst im NW und eine Grabenstruktur im SE. Das komplexe Störungsnetz des Unterhaching Störungssystem ist Zielstruktur verschiedener erfolgreicher Tiefengeothermie-Erschließungsvorhaben.
Putzbrunn-Baldham Fault
Putzbrunn-Baldham Störung
SW-NE to WSW-ENE trending, largely vertical normal fault with a minor offset, forming the southeastern flank of a local graben structure widening toward NE.
SW-NE bis WSW-ENE verlaufende, großteils vertikale Abschiebung. Diese Störung mit relativ geringer Sprunghöhe bildet die südöstliche Verwerfungsebene einer sich nach NE hin verbreiternden lokalen Grabenstruktur.
Taufkirchen-Parsdorf Störung
Taufkirchen-Parsdorf Fault
SW-NE trending, approx. 75° SE dipping synthetic normal fault featuring a throw of up to more than 100 m, separating the southward tapering local horst and graben structures. At its northeastern end presumably soft linked with Poing Fault [DE-BY_1087] via a relay ramp.
SW-NE verlaufende, ca. 75° nach SE einfallende synthetische Abschiebung. Diese Störung mit einer Sprunghöhe von bis über 100 m bildet die Grenze zwischen den sich südwestwärts verengenden Horst (im NW) und Graben (im SE) Strukturen. Am nordöstlichen Ende vermutlich über eine Relais Rampe (relay ramp) mit der Poing Störung [DE-BY_1087] verbunden.
Unterhaching Fault
Unterhaching Störung
SSW-NNE striking, approx. 75° WNW dipping antithetic normal fault featuring a throw of up to ca. 100 m, dwindling in a horsetail splay towards its north. Northwestern edge of a narrow, ramp-like local horst structure.
SSW-NNE streichende, ca. 75° nach WNW einfallende antithetische Abschiebung; nach N hin auffiedernd (horsetail splay). Nordwestliche Flanke einer schmalen, rampenförmigen Horst-Struktur.
Berg-Oberhaching Fault
Berg-Oberhaching Störung
W-E to SW-NE trending, averaged approx. 75° S to SE dipping synthetic normal fault transitioning into Unterhaching Fault System in its northeast.
W-E bis SW-NE verlaufende, im Mittel ca. 75° nach S bis SE einfallende synthetische Abschiebung. Im NE Übergang in das Unterhaching Störungssystem.
Kirchstockach Fault
Kirchstockach Störung
Deining Subfault
Deining Nebenstörung
WNW-ESE striking, approx. 70° SSW dipping synthetic normal fault connecting Berg-Oberhaching [DE-BY_721], Tutzing-Icking [DE-BY_803] and Münsing-Brunnthal [DE-BY_808] synthetic normal faults with unknown kinematics.
WNW-ESE streichende, ca. 70° nach SSW einfallende synthetische Abschiebung. Kinematisch ungeklärte Verbindung der synthetischen Abschiebungen Berg-Oberhaching [DE-BY_721], Tutzing-Icking [DE-BY_803] und Münsing-Brunnthal [DE-BY_808].
Polling-Eberfing Fault
Polling-Eberfing Störung
WNW-ESE streichende, ca. 85° nach SSE einfallende synthetische Abschiebung.
Benningen-Kammlach Fault
Benningen-Kammlach Störung
SW-NE streichende, in etwa 60° nach SE einfallende synthetische Abschiebung.
Forst Bayerdiessen-Wielenbach Fault
Forst Bayerdießen-Wielenbach Störung
Southward arcuate, WNW-ESE to W-E trending, approx. 65° NNE to N dipping antithetic normal fault running from Forst Bayerdiessen to Witzhofen.
Südwärts gebogen, WNW-ESE bis W-E verlaufende, ca. 65° nach NNE bis N einfallende antithetische Abschiebung zwischen Forst Bayerdießen und Witzhofen.
Memmingen Fault
Memmingen Störung
Kinked SW-NE trending, approx. 45° SE dipping synthetic normal fault.
Geknickt SW-NE verlaufende, in etwa 45° nach SE einfallende synthetische Abschiebung.
Wessobrunn-Weilheim Fault
Wessobrunn-Weilheim Störung
Southward arcuate, WNW-ESE to W-E trending, approx. 65° NNE to N dipping antithetic normal fault running from Haid to Unterhausen.
Südwärts gebogen, WNW-ESE bis W-E verlaufende, ca. 65° nach NNE bis N einfallende antithetische Abschiebung zwischen Haid und Unterhausen.
Grossbergham-Lochen Fault
Großbergham-Lochen Störung
WNW-ESE striking, approx. 70° SSW dipping synthetic normal fault north of Seeon; possibly branch of Obing-Altenmarkt Fault [DE-BY_857].
WNW-ESE streichende, ca. 70° nach SSW einfallende synthetische Abschiebung nördlich von Seeon; möglicherweise Zweig der Obing-Altenmarkt Störung [DE-BY_857].
Otterfing-Emertsham Train of Faults
Otterfing-Emertsham Störungszug
Train of faults running from Otterfing N of Holzkirchen in the west to Emertsham NW of Trostberg in the east. Undulate overall WSW-ENE trending array of, steeply ± SSE dipping antithetic normal faults forming the structural traps of various oil- and gasfields.
Von Otterfing (nördlich Holzkirchen) im Westen bis nach Emertsham (nordwestlich von Trostberg) im Osten ziehender Störungszug wellenförmig, insgesamt WSW-ENE verlaufender, steil nach ± SSE einfallender antithetischer Abschiebungen als Fallenstrukturen verschiedener Öl- und Gasfelder.
Schnaitsee Fault
Schnaitsee Störung
WSW-ENE trending, approx. 60° NNW dipping antithethic normal fault running from Eiselfing to Emertsham; northern boundary of oil- and gasfield Schnaitsee.
Von Eiselfing nach Emertsham ziehende, WSW-ENE verlaufende, ca. 60° nach NNW einfallende antithetische Abschiebung; nördliche Begrenzung des Öl- und Gasfeld Schnaitsee.
Mattenhofen-Assling Fault
Mattenhofen-Aßling Störung
Northern boundary of oil- and gasfields Mattenhofen and Assling. Undulate WSW-ENE trending, approx. 80° NNW dipping antithethic normal fault running from Otterfing to Ramerberg.
Von Otterfing nach Ramerberg ziehende, leicht wellig WSW-ENE verlaufende, ca. 80° nach NNW einfallende antithetische Abschiebung; nördliche Begrenzung der Öl- und Gasfelder Mattenhofen und Assling.
Weilheim Fault
Weilheim Störung
W-E striking, steeply (85°-60°) S dipping synthetic normal fault.
W-E streichende, steil (85°-60°) nach S einfallende synthetische Abschiebung.
Trostberg Fault
Trostberg Störung
WNW-ESE striking, approx. 60° NNE dipping antithetic normal fault east of Trostberg.
WNW-ESE streichende, ca. 60° nach NNE einfallende antithetische Abschiebung östlich von Trostberg.
Bernried-Dorfen Fault
Bernried-Dorfen Störung
Slightly arcuate overall WSW-ENE trending, approx. 75° SSE dipping synthetic normal fault.
Leicht gebogen, insgesamt WSW-ENE verlaufende, ca. 75° nach SSE einfallende synthetische Abschiebung.
Mörgen-Walkershofen Fault
Mörgen-Walkershofen Störung
SSW-NNE striking, approx. 75° ESE dipping synthetic normal fault.
SSW-NNE streichende, ca. 75° nach ESE einfallende synthetische Abschiebung.
[lca_050]
W-E striking, approx. 80° N dipping normal fault
W-E streichende, ca. 80° nach N einfallende Abschiebung.
Frauenzell-Bad Wörishofen Fault
Frauenzell-Bad Wörishofen Störung
Slightly undulating, overall SW-NE trending, approx. 55° SE dipping synthetic normal fault from Iller river to Bad Wörishofen.
Leicht wellenförmig, insgesamt SW-NE verlaufende, in etwa 55° nach SE einfallende synthetische Abschiebung zwischen Iller und Bad Wörishofen.
Tuntenhausen-Schönstett Fault
Tuntenhausen-Schönstett Störung
Undulate WSW-ENE trending, approx. 75° NNW dipping antithetic normal fault.
Gewellt WSW-ENE verlaufende, ca. 75° nach NNW einfallende antithetische Abschiebung.
Paterzell Fault
Paterzell Störung
Herrsching-Gauting Fault
Herrsching-Gauting Störung
Slightly northwestward arcuate SW-NE trending, approx. 85° SE dipping synthetic normal fault.
Leicht nordwestwärts gebogene, SW-NE verlaufende, ca. 85° nach SE einfallende synthetische Abschiebung.
St. Leonhard Fault
St. Leonhard Störung
Schwabmünchen Fault
Schwabmünchen Störung
W-E striking, > 85° N dipping antithetic normal fault.
W-E verlaufende, > 85° nach N einfallende antithetische Abschiebung.
Peiting-Peissenberg Fault
Peiting-Peißenberg Störung
Slightly undulate W-E trending, approx. 80° N dipping antithetic normal fault.
Leicht gewellt W-E verlaufende, ca. 80° nach N einfallende antithetische Abschiebung.
Hochzoll-St. Afra Fault
Hochzoll-St. Afra Störung
WNW-ESE streichende, ca. 80° nach NNE einfallende antithetische Abschiebung.
Hohenpeissenberg Fault
Hohenpeißenberg Störung
[lca_056]
[lca_057]
[lca_058]
[lca_059]
W-E streichende, ca. 85° nach S einfallende Abschiebung.
W-E striking, approx. 85° S dipping normal fault
[lca_055]
Pöring Fault
Pöring Störung
Stiefenhofen-Betzigau Fault
Stiefenhofen-Betzigau Störung
WSW-ENE trending, on average approx. 65° NNW dipping antithetic normal fault, probably connected to Möstenberg-Unterthingau Fault [DE-BY_1151].
WSW-ENE verlaufende, durchschnittlich ca. 65° nach NNW einfallende antithetische Abschiebung. Wahrscheinlich mit Möstenberg-Unterthingau Störung [DE-BY_1151] verbunden.
Möstenberg-Unterthingau Fault
Möstenberg-Unterthingau Störung
WSW-ENE striking, approx. 80° NNW dipping antithetic normal fault beneath Kempter Wald.
WSW-ENE streichende, ca. 80° nach NNW einfallende antithetische Abschiebung unter dem Kempter Wald.
Binzenried-Unterthingau Fault
Binzenried-Unterthingau Störung
W-E striking, approx. 70° N dipping antithetic normal fault north of Kempter Wald.
W-E streichende, ca. 70° nach N einfallende antithetische Abschiebung nördlich des Kempter Walds.
Änger-Kempten Fault
Änger-Kempten Störung
W-E striking, approx. 55° SE dipping synthetic normal fault west of Kempten.
W-E streichende, ca. 55° nach S einfallende synthetische Abschiebung westlich von Kempten.
Änger-Probstried Fault
Änger-Probstried Störung
SSW-NNE to SW-NE trending, approx. 85° ESE to SE dipping synthetic normal fault northwest of Kempten.
SSW-NNE bis SW-NE verlaufende, in etwa 85° nach ESE bis SE einfallende synthetische Abschiebung nordwestlich von Kempten.
Unterkürnach-Probstried Fault
Unterkürnach-Probstried Störung
WSW-ENE striking, approx. 70° SSE dipping synthetic normal fault northwest of Kempten.
WSW-ENE streichende, in etwa 70° nach SSE einfallende synthetische Abschiebung nordwestlich von Kempten.
WNW-ESE striking, approx. 60° SSW dipping normal fault
WNW-ESE streichende, ca. 60° nach SSW einfallende Abschiebung.
[lca_060]
Starnberg Fault
Starnberg Störung
Running from Maising to Forstenrieder Park southwest of Munich, SW-NE trending, approx. 85° SE dipping synthetic normal fault. subparallel to antithetic Percha Fault [DE-BY_1092] in the southeast, this probably conjugate pair of faults forms a local graben structure.
Von Maising zum Forstenrieder Park südwestlich von München SW-NE verlaufende, ca. 85° nach SE einfallende synthetische Abschiebung. Subparallel zur antithetischen Percha Störung [DE-BY_1092] im Nordwesten bildet dieses wahrscheinlich konjugierte Störungspaar eine lokale Grabenstruktur.
Percha Fault
Percha Störung
Running from Neusöcking to Forstenrieder Park southwest of Munich, SW-NE trending, approx. 80° NW dipping antithetic normal fault. subparallel to synthetic Starnberg Fault [DE-BY_1093] in the northwest, this probably conjugate pair of faults forms a local graben structure.
Von Neusöcking zum Forstenrieder Park südwestlich von München SW-NE verlaufende, ca. 80° nach NW einfallende antithetische Abschiebung. Subparallel zur synthetischen Starnberg Störung [DE-BY_1093] im Südosten bildet dieses wahrscheinlich konjugierte Störungspaar eine lokale Grabenstruktur.
Lindau-Lindenberg Fault
Lindau-Lindenberg Störung
SW-NE striking, approx. 80° SE dipping synthetic normal fault parallel to Lindau-Hergatz Fault [DE-BY-846].
SW-NE streichende, ca. 85° nach NW einfallende synthetische Abschiebung parallel zur Lindau-Hergatz Störung [DE-BY-846].
Scheidegg-Gestratz Fault
Scheidegg-Gestratz Störung
SW-NE striking, approx. 85° NW dipping antithetic normal fault.
SW-NE streichende, ca. 85° nach NW einfallende antithetische Abschiebung nördlich des Kempter Walds.
Maierhöfen-Röthenbach Fault
Maierhöfen-Röthenbach Störung
SW-NE striking, approx. 65° NW dipping antithetic normal fault.
SW-NE streichende, ca. 65° nach NW einfallende antithetische Abschiebung nördlich des Kempter Walds.
Hohenbrunn-Grasbrunn Fault
Hohenbrunn-Grasbrunn Störung
WSW-ENE trending, approx. 75° SSE dipping synthetic normal fault.
Maierhöfen-Ellhofen Fault
Maierhöfen-Ellhofen Störung
SW-NE verlaufende, ca. 75° nach SE einfallende synthetische Abschiebung.
[lca_067]
WSW-ENE streichende, ca. 50° nach NNW einfallende Abschiebung.
WSW-ENE striking, approx. 50° NNW dipping normal fault
[lca_068]
[lca_069]
[lca_063]
W-E striking, approx. 65° N dipping normal fault
[lca_064]
Ebersberg-Steinhöring Fault
Ebersberg-Steinhöring Störung
WSW-ESE striking, approx. 75° NNW dipping antithetic normal fault.
WSW-ENE streichende, ca. 75° nach NNW einfallende antithetische Abschiebung.
Achering Fault
Achering Störung
Hofoldinger Forst Fault
Hofoldinger Forst Störung
SW-NE striking, approx. 75° NW dipping antithetic normal fault immediate north of and parallel to Otterfing Fault [DE-BY_883].
SW-NE streichende, ca. 75° nach NW einfallende antithetische Abschiebung unmittelbar nördlich parallel zur synthetischen Otterfing Störung [DE-BY_883].
Schwaig-Eitting Fault
Schwaig-Eitting Störung
Otterfing Fault
Otterfing Störung
SW-NE striking, approx. 80° SE dipping synthetic normal fault immediate south of and parallel to antithetic Hofoldinger Forst Fault [DE-BY_884].
SW-NE streichende, ca. 80° nach SE einfallende synthetische Abschiebung unmittelbar südlich parallel zur antithetischen Hofoldinger Forst Störung [DE-BY_884].
Kreuzstrasse-Baiern Fault
Kreuzstraße-Baiern Störung
WSW-ENE to SW-NE striking, approx.75° NNW to NW dipping antithetic normal fault.
WSW-ENE bis SW-NE streichende, ca.75° nach NNW bis NW einfallende antithetische Abschiebung.
Petting Fault
Petting Störung
Slightly undulate WSW-ENE trending, approx. 70° NNW dipping antithetic normal fault east of Traunstein.
Leicht gewellt WSW-ENE verlaufende, ca. 70° nach NNW einfallende antithetische Abschiebung östlich von Traunstein.
Ismaning-Neufinsing Fault
Ismaning-Neufinsing Störung
NW-SE striking, approx. 85° SW dipping normal fault.
NW-SE streichende, ca. 85° nach SW einfallende synthetische Abschiebung.
Traunstein Fault
Traunstein Störung
W-E trending, approx. 50° N dipping antithetic normal fault.
W-E verlaufende, ca. 50° nach N einfallende antithetische Abschiebung.
Ismaning-Zengermoos Cross-fault
Ismaning-Zengermoos Querstörung
Chieming-Nussdorf Fault
Chieming-Nußdorf Störung
Northward arcuate W-E striking, approx. 60° S dipping synthetic normal fault south of the Traunreut Step Fault.
Nordwärts gebogene W-E streichende, ca. 60° nach S einfallende synthetische Abschiebung südlich der Traunreut Bruchstaffel.
Oberschleissheim-Walpertskirchen Fault
Oberschleißheim-Walpertskirchen Störung
WSW-ENE to WNW-ESE trending, averaged approx. 75° ± S dipping synthetic normal fault.
WSW-ENE bis WNW-ESE verlaufende, im Mittel ca. 75° nach ± S einfallende synthetische Abschiebung.
Penzing-Türkenfeld Fault
Penzing-Türkenfeld Störung
Northwestward arcuate WSW-ENE trending, approx. 80° ± NNW dipping antithetic normal fault running from Penzing to south of Geltendorf.
Von Penzing bis südlich Geltendorf ziehende, nordwestwärts gebogen WSW-ENE verlaufende, ca. 80° nach ± NNW einfallende antithetische Abschiebung.
Dietersheim Fault
Dietersheim Störung
WSW-ENE streichende, ca. 70° nach SSE einfallende synthetische Abschiebung.
Buchloe-Landsberg Fault
Buchloe-Landsberg Störung
Slightly arcuate W-E to WSW-ENE trending, approx. 70° S to SSE dipping synthetic normal fault running from Buchloe to Thalhofen.
Leicht gebogen von Buchloe bis Thalhofen ziehende, W-E bis WSW-ENE verlaufende, ca. 70° nach S bis SSE einfallende synthetische Abschiebung.
Eching-Erching Fault
Eching-Erching Störung
WNW-ESE striking, approx. 70° SSW dipping synthetic normal fault.
WNW-ESE streichende, ca. 70° nach SSW einfallende synthetische Abschiebung.
Eichenried-Pretzen Fault
Eichenried-Pretzen Störung
Southward arcuate W-E trending, approx. 65° S dipping synthetic normal fault south of Erding.
Südwärts gebogen W-E verlaufende, ca. 65° nach S einfallende synthetische Abschiebung südlich von Erding.
Erding-Bockhorn Fault
Erding-Bockhorn Störung
Slightly undulate, overall WSW-ENE trending, approx. 70° NNW dipping antithetic normal fault.
Leicht gewellt, insgesamt WSW-ENE verlaufende, ca. 70° nach NNW einfallende antithetische Abschiebung.
Erding Subfault
Erding Nebenstörung
WSW-ENE striking, approx. 70° NNW dipping antithetic normal fault subparallel to synthetic Erding-Altfraunhofen Fault [DE-BY_792], forming a local graben structure.
WSW-ENE streichende, ca. 70° nach NNW einfallende antithetische Abschiebung. Bildet mit der nordwestlich subparallel verlaufenden synthetischen Erding-Altfraunhofen Fault [DE-BY_792] eine lokale Grabenstruktur.
W-E to WSW-ENE trending, approx. 70° N to NNW dipping normal fault
[lca_034]
W-E bis WSW-ENE streichende, ca. 70° nach NNW einfallende Abschiebung.
[lca_035]
WNW-ESE striking, approx. 65° NNE dipping normal fault
[lca_036]
WNW-ESE streichende, ca. 65° nach NNE einfallende Abschiebung.
[lca_037]
WNW-ESE striking, approx. 70° NNE dipping normal fault
WNW-ESE streichende, ca. 70° nach NNE einfallende Abschiebung.
W-E streichende, ca. 75° nach N einfallende Abschiebung.
W-E striking, approx. 75° N dipping normal fault
[lca_030]
[lca_031]
NW-SE streichende, ca. 85° nach NE einfallende Abschiebung.
[lca_032]
NW-SE striking, approx. 85° NE dipping normal fault
[lca_033]
[lca_038]
[lca_039]
SW-NE trending, approx. 70° SE dipping normal fault
Dinkelscherben-Ried Fault
Dinkelscherben-Ried Störung
NW-SE striking, steeply (85°-60°) SW dipping synthetic normal fault.
NW-SE streichende, steil (85°-60°) nach SW einfallende synthetische Abschiebung.
Moosach-Grafing Fault
Moosach-Grafing Störung
Krumbach-Dinkelscherben Fault
Krumbach-Dinkelscherben Störung
SW-NE trending, steeply (85°-60°) NW dipping antithetic normal fault.
SW-NE verlaufende, steil (85°-60°) nach NW einfallende antithetische Abschiebung.
Glonn-Bruck Fault
Glonn-Bruck Störung
Grünbach-Kalling Fault
Grünbach-Kalling Störung
W-E to WNW-ENE trending, approx. 60° ± N dipping antithetic normal fault.
W-E bis WNW-ESE verlaufende, ca. 60° nach ± N einfallende antithetische Abschiebung.
Kirchasch-Algasing Fault
Kirchasch-Algasing Störung
WSW-ENE to WNW-ESE trending, averaged approx. 80° ± S dipping synthetic normal fault.
WSW-ENE bis WNW-ESE verlaufende, im Mittel ca. 80° nach ± S einfallende synthetische Abschiebung.
Wonneberg Fault
Wonneberg Störung
WSW-ENE striking, approx. 70° SSE dipping synthetic normal fault northeast of Traunstein.
WSW-ENE streichende, ca. 70° nach SSE einfallende synthetische Abschiebung nordöstlich von Traunstein.
Neuching-Wörth Fault
Neuching-Wörth Störung
W-E trending, approx. 65° S dipping synthetic normal fault. Kinematic relation to contiguous Markt Schwaben Verwurf [DE-BY_725] unresolved.
W-E verlaufende, ca. 65° nach S einfallende synthetisch Abschiebung. Kinematische Beziehung zum angrenzenden Markt Schwaben Verwurf [DE-BY_725] noch ungeklärt.
Lengdorf Fault
Lengdorf Störung
Arcuate W-ESE striking, approx. 60° N dipping antithetic normal fault.
Bogenförmig W-ESE verlaufende, ca. 60° nach N einfallende antithetische Abschiebung.
Karpfenwinkel Fault
Karpfenwinkel Störung
SW-NE striking, approx. 80° SE dipping synthetic normal fault northwest of Bernried.
SW-NE streichende, ca. 80° nach SE einfallende synthetische Abschiebung nordwestlich von Bernried.
Haselbach-Mickhausen Fault
Haselbach-Mickhausen Störung
[lca_040]
Isen-Ampfing Fault
Ampfinger Hauptstörung
Isen-Ampfing Störung
Overall W-E trending, averaged approx. 55° N dipping antithetic normal fault running from Pastetten to Altmühldorf; northern boundary of oil- and gasfields Isen, Weitermühle-Steinkirchen, and Ampfing.
Von Pastetten nach Altmühldorf ziehende, insgesamt W-E verlaufende, im Durchschnitt ca. 55° nach N einfallende antithetische Abschiebung; nördliche Begrenzung der Öl- und Gasfelder Isen, Weitermühle-Steinkirchen und Ampfing.
Ampfing Subfault
Ampfinger Querstörung
Ampfing Nebenstörung
NW-SE striking, steeply (85°-60°) NE dipping antithetic normal fault close to Ampfing oil- and gasfield.
NW-SE streichende, steil (85°-60°) nach NE einfallende antithesische Abschiebung am Öl- und Gasfeld Ampfing.
Tutzing-Icking Fault
Tutzing-Icking Störung
Slightly undulate WSW-ENE trending, approx. 80° SSE dipping synthetic normal fault.
Leicht gewellt WSW-ENE verlaufende, ca. 80° nach SSE einfallende synthetische Abschiebung.
Stolzenhofen-Hasberg Fault
Stolzenhofen-Hasberg Störung
SW-NE trending, approx. 85° SE dipping synthetic normal fault.
SW-NE verlaufende, ca. 85° nach SE einfallende synthetische Abschiebung.
Walpertskirchen-Dorfen Fault
Walpertskirchen-Dorfen Störung
W-E trending, approx. 70° S dipping synthetic normal fault. At its eastern end subparallel to antithetic Dorfen Fault.
W-E verlaufende, ca.70° nach S einfallende synthetische Abschiebung, in ihrem östichen Teil subparallel zur antithetischen Dorfen Störung.
Reichau-Hasberg Fault
Reichau-Hasberg Störung
SW-NE striking, approx.75° SE dipping synthetic normal fault probably linked to Aletshausen-Langenneufnach Fault [DE-BY_1208] via a relay ramp.
SW-NE streichende, ca. 75° nach SE einfallende synthetische Abschiebung; wahrscheinlich über eine Relais Rampe (relay ramp) mit der Aletshausen-Langenneufnach Störung [DE-BY_1208] verbunden.
Dorfen Fault
Dorfen Störung
W-E trending, approx. 55° N dipping antithetic normal fault running from Dorfen to Schwindegg; northern boundary of oil- and gasfields Dorfen und Dorfen-Ost.
Von Dorfen bis Schwindegg W-E verlaufende, ca. 55° nach N einfallende antithetische Abschiebung; nördliche Begrenzung der Öl- und Gasfelder Dorfen und Dorfen-Ost.
Aletshausen-Langenneufnach Fault
Aletshausen-Langenneufnach Störung
SW-NE to WSW-ENE trending, approx. 75° SE to SSE dipping synthetic normal fault probably linked to Reichau-Hasberg Fault [DE-BY_1209] via a relay ramp.
SW-NE bis WSW-ENE verlaufende, ca. 75° nach SE bis SSE einfallende synthetische Abschiebung; wahrscheinlich über eine Relais Rampe (relay ramp) mit der Reichau-Hasberg Störung [DE-BY_1209] verbunden.
Münsing-Brunnthal Fault
Münsing-Brunnthal Störung
Undulate SW-NE to W-E trending, approx. 75° SE to S dipping synthetic normal fault.
Gewellt SW-NE bis W-E verlaufende, ca. 75° nach SE bis S einfallende synthetische Abschiebung.
Dettenhausen-Sauerlach Subfault
Dettenhausen-Sauerlach Nebenstörung
SW-NE striking, approx. 75° SE dipping synthetic normal fault. Branch of Münsing-Brunnthal Fault [DE-BY_808].
SW-NE streichende, ca. 75° nach SE einfallende synthetische Abschiebung. Zweig der Münsing-Brunnthal Störung [DE-BY_808].
Icking-Deining Lateral Fault
Icking-Deining Querstörung
W-E striking, approx. 85° S dipping synthetic normal fault obtuse-angled to Münsing-Brunnthal Fault [DE-BY_808].
W-E streichende, ca. 85° nach S einfallende synthetische Abschiebung stumpfwinklig zur Münsing-Brunnthal Störung [DE-BY_808].
Kirchhaslach-Aletshausen Fault
Kirchhaslach-Aletshausen Störung
SW-NE striking, approx. 60° NW dipping antithetic normal fault.
SW-NE streichende, ca. 60° nach NW einfallende antithetische Abschiebung.
Grafing-Wasserburg Fault
Grafing-Wasserburg Störung
[lca_046]
[lca_045]
[lca_085]
[lca_047]
[lca_048]
[lca_041]
[lca_042]
WNW-ESE streichende, ca. 80° nach SSW einfallende Abschiebung.
[lca_043]
WNW-ESE striking, approx. 80° SSW dipping normal fault
[lca_044]
All named tectonic boundary objects that are located (at least partly) in Austria, are identified by an ID with the prefix „IS“ listed in the notation.
Instance of a fault or a fissure displayed in the HIKE fault database, as they are represented in the Geological Map of Iceland at 1:600 000 scale and selected faults and fissures on Iceland’s Insular Shelf and Adjacent Deep Ocean
Tectonic Boundary in Iceland
Eyjafjarðaráll Rift Zone
From western end of the Húsavík-Flatey Fault zone to the Kolbeinsey Ridge
Húsavík-Flatey Transform Zone
From Húsavík to the Eyjafjarðaráll Rift
Borgarfjörður Zone
Between Snæfellsnes Volcanic Zone and the Central Volcanic Zone
Grímsey Oblique Rift
From Öxarfjörður to the Kolbeinsey Ridge
Grímsey Earthquake Fault Set
Earthquake faults in the Grímsey Earthquake Fault set
Grímsey Strike-slip Fault Set
Strike-slip faults in the Grímsey earthquake fault set
Stóragrunn Fault and Fissure Sets
Faults and fissures in the Stóragrunn fissure swarm
Stóragrunn Fissure Set
Fissures in the Stóragrunn fissure swarm
Stóragrunn Fault Set
Faults in the Stóragrunn fissure swarm
Nafir Fault Set
Faults in the Nafir fissure swarm
Hóllinn Fault and Fissure Sets
Faults and fissures in the Hóllinn fissure swarm
Hóllinn Fault Set
Faults in the Hóllinn fissure swarm
Hóllinn Fissure Set
Fissures in the Hóllinn fissure swarm
Mánáreyjar Fissure Set
Fissures in the Mánáreyjar fissure swarm
Skjálfandi Fault Set
Faults in the Skjálfandi fissure swarm
Western Volcanic Zone
Reaches from the Reykjanes Oblique Rift northeast to Hofsjökull glacier
Þingvellir Fault and Fissure Sets
Faults and fissures in the Þingvellir fissure swarm
Þingvellir Fault Set
Faults in the Þingvellir fissure swarm
Þingvellir Fissure Set
Fissures in the Þingvellir fissure swarm
Prestahnúkur Fault Set
Faults in the Prestahnúkur fissure swarm
Hveravellir Fault and Fissure Sets
Faults and fissures in the Hveravellir fissure swarm
Hveravellir Fault Set
Faults in the Hveravellir fissure swarm
Hveravellir Fissure Set
Fissures in the Hveravellir fissure swarm
South-Iceland Seismic Transform Zone
Between Reykjanes Oblique Rift and the Eastern Volcanic Zone
Snæfellsnes Volcanic Zone
Located on the Snæfellsnes Peninsula in the west of Iceland
Ljósufjöll Fault and Fissure Sets
Faults and fissures in the Ljósufjöll fissure swarm
Ljósufjöll Fault Set
Faults in the Ljósufjöll fissure swarm
Ljósufjöll Fissure Set
Fissures in the Ljósufjöll fissure swarm
Lýsuhyrna-Helgrindur Fissure Set
Fissures in the Lýsuhyrna-Helgrindur fissure swarm
Snæfellsjökull Fissure Set
Fissures in the Snæfellsjökull fissure swarm
Eastern Volcanic Zone
From Mýrdalsjökull to Askja north of Vatnajökull
Gjálp Fissure Set
Fissures in the Gjálp fissure swarm
Katla-Eldgjá Fault and Fissure Sets
Faults and fissures in the Katla-Eldgjá fissure swarm
Katla-Eldgjá Fault Set
Faults in the Katla-Eldgjá fissure swarm
Katla-Eldgjá Fissure Set
Fissures in the Katla-Eldgjá fissure swarm
Vonarskarð Fissure Set
Fissures in the Vonarskarð fissure swarm
Hamarinn Fissure Set
Fissures in the Hamarinn fissure swarm
Torfajökull Fissure Set
Fissures in the Torfajökull fissure swarm
Veiðivötn Fault and Fissure Sets
Faults and fissures in the Veiðvötn fissure swarm
Veiðivötn Fissure Set
Fissures in the Veiðivötn fissure swarm
Veiðivötn Fault Set
Faults in the Veiðivötn fissure swarm
Hekla-Vatnafjöll Fissure Set
Fissures in the Hekla-Vatnafjöll fissure swarm
Rauðhólar Fault and Fissure Sets
Faults and fissures in the Rauðhólar fissure swarm
Rauðhólar Fissure Set
Fissures in the Rauðhólar fissure swarm
Rauðhólar Fault Set
Faults in the Rauðhólar fissure swarm
Laki Fault and Fissure Sets
Faults and fissures in the Laki fissure swarm
Laki Fissure Set
Fissures in the Laki fissure swarm
Laki Fault Set
Faults in the Laki fissure swarm
Reykjanes Oblique Rift
Offshore from Geirfuglasker near the tip of the Reykjanes Peninsula to Bláfjöll where it connects with the Western Volcanic Zone and the South-Iceland Seismic Zone
Brennisteinsfjöll Fault and Fissure Sets
Faults and fissures in the Brennisteinsfjöll fissure swarm
Brennisteinsfjöll Fault Set
Faults in the Brennisteinsfjöll fissure swarm
Brennisteinsfjöll Fissure Set
Fissures in the Brennisteinsfjöll fissure swarm
Krýsuvík Fault and Fissure Sets
Faults and fissures in the Krýsuvík fissure swarm
Krýsuvík Fault Set
Faults in the Krýsuvík fissure swarm
Krýsuvík Fissure Set
Fissures in the Krýsuvík fissure swarm
Geirfuglasker Fault Set
Faults in the Geirfuglasker fissure swarm
Reykjanes-Eldvörp-Svartsengi Fault and Fissure Sets
Faults and fissures in the Reykjanes-Eldvörp-Svartsengi fissure swarm
Reykjanes-Eldvörp-Svartsengi Fissure Set
Fissures in the Reykjanes-Eldvörp-Svartsengi fissure swarm
Reykjanes-Eldvörp-Svartsengi Fault Set
Faults in the Reykjanes-Eldvörp-Svartsengi fissure swarm
Eldey Fault and Fissure Sets
Faults and fissures in the Eldey fissure swarm
Eldey Fissure Set
Fissures in the Eldey fissure swarm
Eldey Fault Set
Faults in the Eldey fissure swarm
Reykjanes Earthquake Fault Set
Earthquake faults in the Reykjanes Earthquake Fault set
Reykjanes Strike-slip faults
Strike-slip faults in the Reykjanes earthquake fault set
Northern Volcanic Zone
From Vatnajökull to the north coast
Fremri-Námar Fault and Fissure Sets
Faults and fissures in the Fremri-Námar fissure swarm
Fremri-Námar Fault Set
Faults in the Fremri-Námar fissure swarm
Fremri-Námar Fissure Set
Fissures in the Fremri-Námar fissure swarm
Hrúthálsar Fault and Fissure Sets
Faults and fissures in the Hrúthálsar fissure swarm
Hrúthálsar Fissure Set
Fissures in the Hrúthálsar fissure swarm
Hrúthálsar Fault Set
Faults in the Hrúthálsar fissure swarm
Blikalón Fault and Set
Faults in the Blikalón fissure swarm
Kverkfjöll Fault and Fissure Sets
Faults and fissures in the Kverkfjöll fissure swarm
Kverkfjöll Fissure Set
Fissures in the Kverkfjöll fissure swarm
Kverkfjöll Fault Set
Faults in the Kverkfjöll fissure swarm
Þeistareykir Fault and Fissure Sets
Faults and fissures in the Þeistareykir fissure swarm
Þeistareykir Fault Set
Faults in the Þeistareykir fissure swarm
Þeistareykir Fissure Set
Fissures in the Þeistareykir fissure swarm
Krafla-Gjástykki Fault and Fissure Sets
Faults and fissures in the Krafla-Gjástykki fissure swarm
Krafla-Gjástykki Fissure Set
Fissures in the Krafla-Gjástykki fissure swarm
Krafla-Gjástykki Fault Set
Faults in the Krafla-Gjástykki fissure swarm
Askja Fault and Fissure Sets
Faults and fissures in the Askja fissure swarm
Askja Fault Set
Faults in the Askja fissure swarm
Askja Fissure Set
Fissures in the Askja fissure swarm
Central Volcanic Zone
Surrounding Hofsjökull glacier between Western and Eastern Volcanic Zone
Kerlingarfjöll Fault Set
Faults in the Kerlingarfjöll fissure swarm
Hofsjökull Fault Set
Faults in the Hofsjökull fissure swarm
All named tectonic boundary objects that are located (at least partly) in Italy, are identified by an ID with the prefix „IT“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Italy as they appear on the HIKE European fault database. They are sorted into fault systems or tectonic domains.
Tectonic Boundary in Italy
Ortona-Roccamonfina Lineament
Linea Ortona-Roccamonfina
The Ortona-Roccamonfina (or Sangro-Volturno) lineament is considered the tectonic separation between the northern Apennines and and Southern Apennines (Patacca & Scandone, 2007 and references therein). The Ortona-Roccamonfina transversal structure can be interpreted as a crustal oblique thrust ramp, trending NNE-SSW, with right-lateral transpressive kinematic involving the Apulian carbonate platform and the slope-to-basin paleodomains. Thrusts and related folds of the Ortona-Roccamonfina oblique ramp also involve the basal thrust and the left-lateral oblique ramp of the Molise Allocthonous Units (Satolli et al., 2014).
La Linea Ortona-Roccamonfina (o Sangro-Volturno) è considerata la separazione tra l'Appennino settentrionale e quello meridionale (Patacca & Scandone, 2007 e bibliografia inclusa). Questa struttura trasversale può essere interpretata come una rampa crostale obliqua, ad andamento NNE-SSO, con cinematica transpressiva destra, che coinvolge la piattaforma carbonatica Apula e i paleodomini di scarpata-bacino. Sovrascorrimenti e pieghe associate con questa rampa obliqua coinvolgono anche il sovrascorrimento basale e la rampa laterale obliqua sinistra delle Unità alloctone molisane (Satolli et al., 2014).
Adriatic plate passive continental margin Domain
Dominio del margine continentale passivo della placca Adriatica
The Adriatic plate passive continental margin domain is characterized by normal faults, mainly NNW-SSE and N-S oriented, steeply W- and E-dipping. Minor W-E and NE-SW faults are present. These faults are related to the rifting phase affecting the Adriatic/Africa plate margin during Late Triassic and from Early Jurassic to Early Cretaceous (Masetti et al, 2012).
Il dominio del margine continentale passivo della placca Adriatica è caratterizzato da faglie normali, ad andamento prevalente SSE-NNO e N-S, molto inclinate verso E e O. Meno frequentemente sono presenti anche faglie ad andamento E-O e NE-SO. Queste faglie sono legate alla fase di rifting che ha interessato il margine della placca Adriatica nel Triassico superiore e dal Giurassico inferiore fino al Cretacico inferiore (Masetti et al, 2012).
Bedizzole Fault System
Sistema di faglie Bedizzole
NE-SW trending fault system characterized by NW- and SE-dipping normal faults.
Sistema di faglie normali ad andamento NE-SO con inclinazione verso NO e SE.
Bedizzole 3 Fault
Faglia Bedizzole 3
NNE-SSW trending normal fault with a steep ESE dip.
Faglia normale ad andamento NNE-SSO molto inclinata verso ESE.
Bedizzole 2 Fault
Faglia Bedizzole 2
NE-SW trending normal fault with a steep north-west dip.
Faglia normale ad andamento NE-SO molto inclinata verso NO.
Bedizzole 1 Fault
Faglia Bedizzole 1
Nogara Fault System
Sistema di faglie Nogara
SE-NW trending fault system characterized by steeply SW- and NE-dipping normal faults.
Sistema di faglie normali ad andamento da SE-NO con inclinazione verso SO e NE.
Nogara 2 antithetic Fault
Faglia Nogara 2 antitetica
SE-NW trending normal fault steeply NE-dipping.
Faglia normale ad andamento SE-NO molto inclinata verso NE.
Nogara 2 Fault
Faglia Nogara 2
ESE-WNW trending normal fault steeply SSW-dipping.
Faglia normale ad andamento ESE-ONO molto inclinata verso SSO.
Nogara 9 Fault
Faglia Nogara 9
SSE-NNW trending normal fault steeply WSW-dipping.
Faglia normale ad andamento SSE-NNO molto inclinata verso OSO.
Nogara 3 antithetic Fault
Faglia Nogara 3 antitetica
Nogara 8 Fault
Faglia Nogara 8
SE-NW trending normal fault steeply SW-dipping.
Faglia normale ad andamento SE-NO molto inclinata verso SO.
Nogara 3 Fault
Faglia Nogara 3
Nogara 6 antithetic Fault
Faglia Nogara 6 antitetica
ESE-WNW trending normal fault steeply NNE-dipping.
Faglia normale ad andamento ESE-ONO molto inclinata verso NNE.
Nogara 4 antithetic Fault
Faglia Nogara 4 antitetica
Nogara 6 Fault
Faglia Nogara 6
Nogara 4 Fault
Faglia Nogara 4
Nogara 5 Fault
Faglia Nogara 5
Nogara 5 antithetic Fault
Faglia Nogara 5 antitetica
Nogara 7 Fault
Faglia Nogara 7
SE-NW trending vertical normal fault SW-dipping.
Faglia normale subverticale ad andamento SE-NO inclinata verso SO.
Nogara 1 antithetic Fault
Faglia Nogara 1 antitetica
Nogara Fault
Faglia Nogara
Nogara 1 Fault
Faglia Nogara 1
Virgilio Fault
Faglia Virgilio
N-S trending normal fault with steep west dip.
Faglia normale ad andamento N-S molto inclinata verso ovest.
Asola Fault System
Sistema di faglie Asola
SSE-NNW trending fault system characterized by ENE- and WSW-dipping normal faults.
Sistema di faglie normali ad andamento SSE-NNO con inclinazione verso ENE e OSO.
Asola 5 Fault
Faglia Asola 5
SSE-NNW trending normal fault with a steep WSW dip.
Asola 4 Fault
Faglia Asola 4
Asola 3 Fault
Faglia Asola 3
SE-NW trending normal fault with a steep SW dip.
Asola 2 Fault
Faglia Asola 2
Asola 1 Fault
Faglia Asola 1
Asola 1 antithetic Fault
Faglia Asola 1 antitetica
SSE-NNW trending normal fault with a steep ENE dip.
Faglia normale ad andamento SSE-NNO molto inclinata verso ENE.
Castiglione Fault System
Sistema di faglie Castiglione
ESE-WNW trending fault system characterized by SSW-dipping normal faults.
Sistema di faglie normali ad andamento ESE-ONO con inclinazione verso SSO.
Castiglione Fault
Faglia Castiglione
ESE-WNW trending normal fault with a steep SSW dip.
Castiglione 3 Fault
Faglia Castiglione 3
Castiglione 2 Fault
Faglia Castiglione 2
Castiglione 1 Fault
Faglia Castiglione 1
Gambara Fault System
Sistema di faglie Gambara
N-S to NNE-SSW trending fault system characterized by W-and E-dipping normal faults.
Sistema di faglie normali ad andamento da N-S a NNE-SSO con inclinazione verso ovest e verso est.
Gambara 1 Fault
Faglia Gambara 1
Gambara 2 Fault
Faglia Gambara 2
SSE-NNW trending nornal fault with a steep WSW dip.
Gambara 5 Fault
Faglia Gambara 5
Gambara 6 Fault
Faglia Gambara 6
Gambara 7 Fault
Faglia Gambara 7
NNE-SSW trending normal fault with a steep WNW dip.
Faglia normale ad andamento NNE-SSO molto inclinata verso ONO.
Gambara 8 Fault
Faglia Gambara 8
Gambara 11 Fault
Faglia Gambara 11
ENE-WSW trending normal fault with a steep SSE dip.
Faglia normale ad andamento ENE-OSO molto inclinata verso SSE.
Gambara 10 Fault
Faglia Gambara 10
Gambara 9 Fault
Faglia Gambara 9
Gambara 4 Fault
Faglia Gambara 4
Gambara 3 Fault
Faglia Gambara 3
Viadana Fault System
Sistema di faglie Viadana
SE-NW trending fault system characterized by normal faults steeply SW-dipping.
Sistema di faglie normali ad andamento da SE-NO con inclinazione verso SO.
Viadana 3 Fault
Faglia Viadana 3
Viadana 6 Fault
Faglia Viadana 6
Viadana 4 Fault
Faglia Viadana 4
Viadana Fault
Faglia Viadana
Viadana 1 Fault
Faglia Viadana 1
Viadana 2 Fault
Faglia Viadana 2
Rodigo Fault System
Sistema di faglie Rodigo
SSE-NNW trending fault system characterized by steeply WSW- and ENE-dipping normal faults.
Sistema di faglie normali ad andamento da SSE-NNO con inclinazione verso OSO e ENE.
Rodigo 2 Fault
Faglia Rodigo 2
SE-NW trending normal fault with a steep south-west dip.
Rodigo 1 Fault
Faglia Rodigo 1
N-S trending normal fault with a steep west dip.
Faglia normale ad andamento N-S molto inclinata verso O.
Rodigo Fault
Faglia Rodigo
Rodigo 1 antithetic Fault
Faglia Rodigo 1 antitetica
Rodigo 3 Fault
Faglia Rodigo 3
Rodigo 4 Fault
Faglia Rodigo 4
SSE-NNW trending vertical normal fault with a WSW dip.
Faglia normale subverticale ad andamento SSE-NNO inclinata verso OSO.
Garlasco Fault System
Sistema di faglie Garlasco
N-S trending fault system characterized by E-dipping normal faults.
Sistema di faglie normali ad andamento da N-S con inclinazione verso est.
Garlasco 1 Fault
Faglia Garlasco 1
N-S trending normal fault with an intermediate east dip.
Faglia normale ad andamento N-S molto inclinata verso est.
Garlasco 2 Fault
Faglia Garlasco 2
SSE-NNW trending normal fault with an intermediate east dip.
Faglia normale ad andamento SSE-NNO molto inclinata verso est.
Piadena Fault System
Sistema di faglie Piadena
Piadena 1 Fault
Faglia Piadena 1
Piadena 2 Fault
Faglia Piadena 2
Piadena 3 Fault
Faglia Piadena 3
Piadena Fault
Faglia Piadena
Piadena 1 antithetic Fault
Faglia Piadena 1 antitetica
SE-NW trending normal fault with a steep NE dip.
Piadena 4 Fault
Faglia Piadena 4
Mantova Fault System
Sistema di faglie Mantova
NE-SW trending fault system characterized by SE-dipping normal faults.
Sistema di faglie normali ad andamento da NE-SO con inclinazione verso SE.
Mantova Fault
Faglia Mantova
NE-SW trending vertical normal fault with a south-east dip.
Faglia normale subverticale ad andamento NE-SO inclinata verso SE.
Mantova 1 Fault
Faglia Mantova 1
ENE-WSW trending normal fault with a steep south dip.
Faglia normale ad andamento ENE-OSO molto inclinata verso sud.
Mantova 2 Fault
Faglia Mantova 2
Gaggiano Fault System
Sistema di faglie Gaggiano
N-S trending fault system characterized by W-and E-dipping normal faults.
Sistema di faglie normali ad andamento N-S con inclinazione verso ovest e verso est.
Gaggiano 2 Fault
Faglia Gaggiano 2
N-S trending normal faults with an intermediate east dip.
Faglia normale ad andamento N-S mediamente inclinata verso est.
Gaggiano 1 Fault
Faglia Gaggiano 1
Gaggiano 3 Fault
Faglia Gaggiano 3
Gaggiano 4 Fault
Faglia Gaggiano 4
N-S trending nvertical ormal faults with a west dip.
Faglia normale subverticale ad andamento N-S inclinata verso ovest.
Gaggiano 5 Fault
Faglia Gaggiano 5
NNE-SSE trending normal fault with an interemediate ESE dip.
Faglia normale ad andamento SSE-NNO mediamente inclinata verso ESE.
Suzzara Fault System
Sistema di faglie Suzzara
Suzzara 2 antithetic Fault
Faglia Suzzara 2 antitetica
Suzzara Fault
Faglia Suzzara
Suzzara 1 antithetic Fault
Faglia Suzzara 1 antitetica
Suzzara 2 Fault
Faglia Suzzara 2
N-S trending normal fault with a steep east dip.
Suzzara 1 Fault
Faglia Suzzara 1
Il Dominio del bacino di avampaese Padano-Adriatico è caratterizzato da sovrascorrimenti sepolti e/o ciechi evidenziati unicamente da indagini sismiche e perforazioni profonde. Esso ha rappresentato il bacino di avampaese sia per la catena Alpina (retrovergente) che per quella Appenninica Settentrionale; per questo motivo i sovrascorrimenti hanno immersioni e vergenze opposte: immersione verso N e vergenza a S, per la catena Alpina (Sudalpino), e immersione da S a SO e vergenza da N a NE, per la catena Appenninica. La loro attività è compresa tra il Cattiano e il presente. I principali sovrascorrimenti sono caratterizzati da una forma arcuata con un andamento, spostandosi da ovest a est/sud-est: principalmente O-E (Alpi Occidentali e Sudalpino, Fronte del Monferrato e Arco Emiliano), NO-SE (Arco Ferrara-Romagna) e NNO-SSE i sovrascorrimenti adriatici. Sono anche riconosciuti alcuni sovrasocrrimenti minori e isolati NE-vergenti.
The Po Plain-Adriatic foreland basin domain is characterized by buried and/or blind thrusts solely evidenced by seismic surveys and deep drillings. It represented the common foreland basin of both Alps (retroforeland) and Northern Apennines fold-and-thrust belts; for this reason the thrusts are N-dipping S-vergent and S- to SW-dipping N- to NE-vergent, respectively those of the retrobelt of the Alps (Southern Alps) and of the Apennines front. Their activity ranges from Chattian to present. The main thrust fronts are characterized by an arcuated shape with the following trend, moving from west to east and south-east: mainly E-W (Western and Southern Alps, Monferrato Front and Emilia arc), SE-NW (Ferrara-Romagna arc) and SSE-NNW the adriatic thrusts. Some minor isolated thrust NE-vergent are also recognized.
Po Plain-Adriatic foreland basin Domain
Dominio del bacino di avampaese padano-adriatico
Lombardia Arc subdomain
Arco Lombardo
The Lombardia Arc subdomain is characterized by thrusts connected to the south-verging retrobelt of the Alps (i.e. Southern Alps). The thrusts and back-thrusts have a mainly E-W trend. Two different décollement levels characterize these thrusts: the deeper in correspondence of Triassic evaporites (L1), the shallower in correspondence of the Eocene-Oligocene marly units (L2). The southward propagation of these structures occurred during Late Cretaceous, with major shortening occurring during Oligocene and Miocene.
Il sottodominio dell'Arco Lombardo è caratterizzato da sovrascorrimenti legati alla catena Alpina sud-vergente (Sudalpino). I sovrascorrimenti e i retroscorrimenti hanno prevalentemente direzione E-O. I sovrascorrimenti sono caratterizzati da due diversi livelli di scollamento: il più profondo in corrispondenza delle evaporiti triassiche (L1), il più superficiale in corrispondenza delle unità marnose di età variabile tra l'Eocene e l'Oligocene (L2). La migrazione verso sud delle strutture è avvenuta durante il Cretacico superiore, con i maggiori raccorciamenti durante l'Oligocene e il Miocene.
Malpaga Thrust
Sovrascorrimento Malpaga
E-W trending thrust fault with an intermediate north dip. The décollement level is L1.
Sovrascorrimento ad andamento E-O mediamente inclinato verso nord. Il livello di scollamento è L1.
San Gervasio Thrust Splay
Sovrascorrimento secondario San Gervasio
E-W trending thrust fault with a gentle north dip. The décollement level is L2.
Sovrascorrimento ad andamento E-O debolmente inclinato verso nord. Il livello di scollamento è L2.
Crema 1 Trust
Sovrascorrimento Crema 1
E-W to N-S trending thrust fault, gentle dipping toward NE. The décollement level is L2.
Sovrascorrimento ad andamento da E-O a N-S debolmente inclinato verso NE. Il livello di scollamento è L2.
Crema 3 Thrust
Sovrascorrimento Crema 3
SSE-NNW trending thrust fault with a gentle ENE dip. The décollement level is L2.
Sovrascorrimento ad andamento SSE-NNO debolmente inclinato verso ENE. Il livello di scollamento è L2.
Soncino Thrust
Sovrascorrimento Soncino
ESE-WNW trending fault with a gentle NNE dip. The décollement level is L1.
Sovrascorrimento ad andamento ESE-ONO debolmente inclinato verso NNE. Il livello di scollamento è L1.
San Gervasio back-thrust
Retroscorrimento San Gervasio
E-W trending thrust fault with an intermediate south dip. It is a back-thrust associated with the San Gervasio thrust.The décollement level is L2.
Sovrascorrimento ad andamento E-O mediamente inclinato verso sud. È un retroscorrimento associato al Sovrascorrimento San Gervasio. Il livello di scollamento è L2.
Ponterosso Thrust
Sovrascorrimento Ponterosso
ENE-WSW trending thrust fault with a gentle NNW dip. The décollement level is L2.
Sovrascorrimento ad andamento ENE-OSO debolmente inclinato verso NNO. Il livello di scollamento è L2.
Sirmione Thrust
Sovrascorrimento Sirmione
Maclodio 2 Thrust
Sovrascorrimento Maclodio 2
ESE-WNW trending thrust fault with an intermediate NNE dip. The décollement level is L2.
Sovrascorrimento ad andamento ESE-ONO mediamente inclinato verso NNE. Il livello di scollamento è L2.
Brescia Thrust splay
Sovrascorrimento secondario Brescia
ESE-WNW trending thrust fault with an intermediate NNE dip. The décollement level is L1.
Sovrascorrimento ad andamento ESE-ONO mediamente inclinato verso NNE. Il livello di scollamento è L1.
Borgosatollo Thrust
Sovrascorrimento Borgosatollo
ENE-WSW trending thrust fault with an intermediate NNW dip. The décollement level is L2.
Sovrascorrimento ad andamento ENE-OSO mediamente inclinato verso NNO. Il livello di scollamento è L2.
Maclodio 1 Thrust
Sovrascorrimento Maclodio 1
E-W trending thrust fault with an intermediate north dip. The décollement level is L2.
Sovrascorrimento ad andamento E-O mediamente inclinato verso nord. Il livello di scollamento è L2.
Crema Thrust
Sovrascorrimento Crema
Solferino Thrust
Sovrascorrimento Solferino
E-W trending thrust fault with a intermediate north dip. The décollement level is L1.
San Gervasio Thrust
Sovrascorrimento San Gervasio
E-W to N-S trending thrust fault gentle NNW dipping. The décollement level is L2.
Sovrascorrimento ad andamento da E-O a N-S debolmente inclinato verso NNO. Il livello di scollamento è L2.
San Bartolomeo Thrust
Sovrascorrimento San Bartolomeo
E-W trending thrust fault with a gentle north dip. The décollement level is L1.
Sovrascorrimento ad andamento E-O debolmente inclinato verso nord. Il livello di scollamento è L1.
Crema 2 Thrust
Sovrascorrimento Crema 2
Campazzo Thrust
Sovrascorrimento Campazzo
Verolanuova Thrust
Sovrascorrimento Verolanuova
Capriano del Colle Thrust
Sovrascorrimento Capriano del Colle
ESE-WNW trending thrust fault with an intermediate SSW dip. The décollement level is L2.
Sovrascorrimento ad andamento ESE-ONO mediamente inclinato verso SSO. Il livello di scollamento è L2.
Bagnolo Mella Thrust
Sovrascorrimento Bagnolo Mella
ESE-WNW trending thrust fault with a gentle NNE dip. The décollement level is L2.
Sovrascorrimento ad andamento ESE-ONO debolmente inclinato verso NNE. Il livello di scollamento è L2.
Ghedi Thrust
Sovrascorrimento Ghedi
Castenedolo Thrust
Sovrascorrimento Castenedolo
ESE-WNW trending thrust fault with a gentle SSW dip. The décollement level is L2.
Sovrascorrimento ad andamento ESE-ONO debolmente inclinato verso SSO. Il livello di scollamento è L2.
Manerbio Thrust
Sovrascorrimento Manerbio
NE-SW trending thrust fault with a gentle NW dip. The décollement level is L2.
Sovrascorrimento ad andamento NE-SO debolmente inclinato verso NO. Il livello di scollamento è L2.
Brescia Thrust
Sovrascorrimento Brescia
Emilia Arc subdomain
Sottodominio Arco Emiliano
The Emilia Arc subdomain is the central arc of the Northern Apennines. It is a mainly north-verging system of thrust faults with related back-thrusts. Two different décollement levels characterize these thrust faults: the deeper in correspondence of Triassic evaporites (L1), the shallower in correspondence of the Eocene-Oligocene to Miocene marly units (L2). The Emilia arc started deforming in the Tortonian, reached its present-day configuration in the Zanclean, and experienced maximum activity in Piacenzian–Gelasian times.
Il sottodominio dell'Arco Emiliano rappresenta la porzione centrale del fronte dell'Appennino Settentrionale. È costituito da sistemi di faglie con sovrascorrimenti e associati retroscorrimenti. Sono riconoscibili due livelli di scollamento: il più profondo in corrispondenza delle evaporiti triassiche (L1), il più superficiale in corrispondenza delle unità marnose di età variabile dall'Eocene-Oligocene al Miocene (L2). La deformazione ha avuto inizio nel Tortoniano; l'Arco ha raggiunto la sua attuale configurazione nello Zancleano, e ha subito la massima deformazione nell'intervallo Piacenziano-Gelasiano.
Caviaga - Pontevico Fault System
Sistema di faglie Caviaga - Pontevico
E-W trending fault system characterized by thrust and back-thrust. The décollement level is L2.
Sistema di faglie caratterizzato da sovrascorrimenti e associati retroscorrrimenti ad andamento E-O. Il livello di scollamento è L2.
Caviaga - Pontevico Thrust
Sovrascorrimento Caviaga - Pontevico
E-W trending thrust fault with a gentle south dip.
Sovrascorrimento ad andamento E-O debolmente inclinato verso sud.
Caviaga - Pontevico back-thrust
Retroscorrimento Caviaga - Pontevico
E-W trending thrust fault with an intermediate north dip. It is a back-thrust associated with the Cornegliano Thrust.
Sovrascorrimento ad andamento E-O mediamente inclinato verso nord. È un retroscorrimento associato al Sovrascorrimento Caviaga - Pontevico.
Cortemaggiore - Cavriago Fault System
Sistema di faglie Cortemaggiore - Cavriago
ESE-WNW trending fault system characterized by thrust and back-thrust. The décollement level is L2.
Sistema di faglie caratterizzato da sovrascorrimenti e associati retroscorrrimenti ad andamento ESE-ONO. Il livello di scollamento è L2.
Parma Thrust
Sovrascorrimento Parma
SE-NW trending thrust fault with an intermediate SW dip.
Sovrascorrimento ad andamento SE-NO mediamente inclinato verso SO.
Cavriago Thrust
Sovrascorrimento Cavriago
ESE-WNW trending thrust fault with a steep SSW dip.
Sovrascorrimento ad andamento ESE-ONO molto inclinato verso SSO.
Cortemaggiore Thrust
Sovrascorrimento Cortemaggiore
ESE-WNW trending thrust fault with an intermediate SSW dip.
Sovrascorrimento ad andamento ESE-ONO mediamente inclinato verso SSO.
Cortemaggiore back-thrust
Retroscorrimento Cortemaggiore
ESE-WNW trending thrust fault with an intermediate NNE dip. It is a back-thrust associated with the Cortemaggiore Thrust.
Sovrascorrimento ad andamento ESE-ONO mediamente inclinato verso NNE. È un retroscorrimento associato al Sovrascorrimento Cortemaggiore.
Castelnovo thrust
Sovrascorrimento Castelnovo
ESE-WNW trending thrust fault gentle SSW-dipping. The décollement level is L2.
Voghera - San Colombano Fault System
Sistema di faglie Voghera - San Colombano
NE-SW to E-W trending fault system constituted by thrust faults with intermediate mostly south dip. The décollement level is L2.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento da NE-SO a E-O, mediamente inclinati prevalentemente verso sud. Il livello di scollamento è L2.
San Colombano Thrust
Sovrascorrimento San Colombano
E-W trending thrust fault with an internediate south dip.
Sovrascorrimento ad andamento E-O mediamente inclinato verso sud.
Voghera - Villanterio Thrust
Sovrascorrimento Voghera - Villanterio
NE-SW thrust fault with intermediate south-east dip.
Sovrascorrimento ad andamento NE-SO mediamente inclinato verso SE.
Solarolo Fault System
Sistema di faglie Solarolo
ESE-WNW trending fault system characterized by thrust faults SSW-dipping. The décollement level is L2.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento ESE-ONO. Il livello di scollamento è L2.
Solarolo 1 Thrust
Sovrascorrimento Solarolo 1
ESE-WNW thrust fault with a gentle SSW-dipping.
Sovrascorrimento ad andamento ESE-ONO debolmente inclinato verso SSO.
Solarolo Thrust
Sovrascorrimento Solarolo
Cremona - Reggio nell'Emilia Fault System
Sistema di faglie Cremona - Reggio nell'Emilia
SE-NW trending fault system characterized by thrust faults with gentle to intermediate south-west dip and associated back-thrusts. The décollement level is L2.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento SE-NO, da debolmente a mediamente inclinati verso SO, con associati retroscorrimenti. Il livello di scollamento è L2.
Cremona Back-Thrust
Retroscorrimento Cremona
ESE-WNW trending thrust fault, intermediate NNE-dipping. It is a back-thrust associated with the Cremona Thrust.
Sovrascorrimento ad andamento ESE-ONO mediamente inclinato verso NNE. È un retroscorrimento associato al Sovrascorrimento Cremona.
Cremona Thrust
Sovrascorrimento Cremona
ESE-WNW trending thrust fault, gentle SSW-dipping.
Parma - Reggio nell'Emilia 1 Thrust
Sovrascorrimento Parma - Reggio nell'Emilia 1
SE-NW trending thrust fault with intermediate south-west dip.
Parma - Reggio nell'Emilia 1 Back-Thrust
Retroscorrimento Parma - Reggio nell'Emilia 1
SE-NW trending thrust fault with steep north-east dip. It is a back-thrust associated with the Parma - Reggio nell'Emilia Thrust 1.
Sovrascorrimento ad andamento SE-NO molto inclinato verso NE. È un retroscorrimento associato al Sovrascorrimento Parma - Reggio nell'Emilia 1.
Lacchiarella Fault System
Sistema di faglie Lacchiarella
N-S trending fault system characterized by thrusts and back-thrusts related to the reactivation and tectonic inversion of former syn-rift Mesozoic (Liassic) normal faults (i.e. Gaggiano Fault System). Reactivation activity spans from Chattian to Tortonian.
Sistema di faglie ad andamento N-S connesso alla riattivazione e all'inversione di faglie normali preesistenti (Sistema di faglie di Gaggiano) legate al rifting mesozoico. La riattivazione è compresa tra il Cattiano e il Tortoniano.
Lacchiarella 2 Thrust
Sovrascorrimento di Lacchiarella 2
N-S trending thrust fault with a gentle eastern dip.
Sovrascorrimento ad andamento N-S debolmente inclinato verso est.
Lacchiarella 1 Thrust
Sovrascorrimento di Lacchiarella 1
NNE-SSW trending thrust fault with a gentle eastern dip.
Sovrascorrimento ad andamento NNE-SSO debolmente inclinato verso est.
Lacchiarella back-thrust
Retroscorrimento di Lacchiarella
N-S trending thrust fault with a gentle western dip. It is a back-thrust associated with Lacchiarella Thrust.
Sovrascorrimento ad andamento N-S debolmente inclinato verso ovest. Si tratta di un retroscorrimento associato al Sovrascorrimento Lacchiarella.
Lacchiarella Thrust
Sovrascorrimento di Lacchiarella
N-S trending thrust fault with an intermediate eastern dip.
Sovrascorrimento ad andamento N-S mediamente inclinato verso est.
Ferrara - Romagna arc subdomain
Arco Ferrara - Romagna
The Ferrara-Romagna Arc subdomain is the eastern arc of the Northern Apennines. It is a mainly SE-dipping fault system of thrusts, related back-thrusts, and oblique slip faults. The thrusts have a ENE-WSW, in the western sector, and ESE-WNW trend, in the eastern sector. Two different décollement levels characterize these thrust faults: the deeper in correspondence of Triassic evaporites (L1), the shallower in correspondence of the Eocene-Oligocene to Miocene marly units (L2). The fault system activity started in the Late Messinian-Early Pliocene; the outward propagation of the thrust fronts continued until the Zanclean–Piacenzian and the Gelasian, moving from the inner to the outer fronts, and is still active.
Il sottodominio dell'Arco Ferrara-Romagna è la porzione più orientale del fronte dell'Appennino Settentrionale. È costiutito da sovrascorrimenti prevalentemente inclinati verso SE, con associati retroscorrimenti e faglie oblique. I sovrascorrimenti hanno andamento ENE-OSO nel settore occidentale, e ESE-ONO nel settore orientale. Sono riconoscibili due livelli di scollamento: il più profondo in corrispondenza delle evaporiti triassiche (L1), il più superficiale in corrispondenza delle unità marnose di età variabile dall'Eocene-Oligocene al Miocene (L2). L'attività è iniziata nel Messiniano superiore - Pliocene inferiore; la migrazione verso l'esterno del fronte è proseguita fino allo Zancleano-Piacenziano e al Gelasiano, spostandosi dai settori più interni verso quelli esterni, ed è tuttora attiva.
Sermide - Copparo Fault System
Sistema di faglie Sermide - Copparo
E-W trending fault system characterized by south-dipping thrust faults.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento E-O inclinati verso sud.
Sermide - Copparo Thrust
Sovrascorrimento Sermide - Copparo
E-W trending thrust fault with a gentle south dip. The décollement level is L1.
Sovrascorrimento ad andamento E-O debolmente inclinato verso sud. Il livello di scollamento è L1.
Mirandola - Consandolo Fault System
Sistema di faglie Mirandola - Consandolo
ESE-WNW trending fault system characterized by thrust, back-thrust and associated oblique slip faults. The décollement level is L1.
Sistema di faglie caratterizzato da sovrascorrimenti e retroscorrrimenti ad andamento ESE-ONO, e associate faglie oblique. Il livello di scollamento è L1.
San Felice minor 2 back-thrust
Retroscorrimento San Felice minore 2
SE-NW trending thrust fault with a steep NE dip. It is a back-thrust associated with the S. Felice inner 2 thrust.
Sovrascorrimento ad andamento SE-NO molto inclinato verso NE. È un retroscorrimento associato con il Sovrascorrimento San Felice interno 2.
San Felice minor 3 back-thrust
Retroscorrimento San Felice minore 3
ESE-WNW trending thrust fault with a steep NNE dip. It is a back-thrust associated with the Mirandola - Consandolo thrust.
Sovrascorrimento ad andamento ESE-ONO molto inclinato verso NNE. È un retroscorrimento associato con il Sovrascorrimento Mirandola - Consandolo.
San Felice minor 4 back-thrust
Retroscorrimento San Felice minore 4
San Felice 1 oblique slip fault
Faglia obliqua San Felice 1
NE-SW trending oblique slip fault with a steep SE dip.
Faglia obliqua ad andamento NE-SO molto inclinata verso SE.
San Felice 2 oblique slip fault
Faglia obliqua San Felice 2
NNE-SSW trending oblique slip vertical fault with a ESE dip.
Faglia obliqua subverticale ad andamento NNE-SSO inclinata verso ESE.
Mirandola - Consandolo thrust
Sovrascorrimento Mirandola - Consandolo
San Felice 3 oblique slip fault
Faglia obliqua San Felice 3
NE-SW trending oblique slip vertical fault with a SE dip.
Faglia obliqua subverticale ad andamento NE-SO inclinata verso SE.
San Felice 1 inner thrust
Sovrascorrimento San Felice interno 1
E-W trending thrust fault with an intermediate south dip.
San Felice 2 inner thrust
Sovrascorrimento San Felice interno 2
San Felice 3 inner thrust
Sovrascorrimento San Felice interno 3
SSE-NNW trending thrust fault with an intermediate WSW dip.
Sovrascorrimento ad andamento SSE-NNO mediamente inclinato verso OSO.
San Felice 4 inner thrust
Sovrascorrimento San Felice interno 4
San Felice minor 1 back-thrust
Retroscorrimento San Felice minore 1
ESE-WNW trending thrust fault with a steep NNE dip. It is a back-thrust associated with the S. Felice inner 1 thrust.
Sovrascorrimento ad andamento ESE-ONO molto inclinato verso NNE. È un retroscorrimento associato con il Sovrascorrimento San Felice interno 1.
Poggio Rusco - Ferrara Fault System
Sistema di faglie Poggio Rusco -Ferrara
E-W trending fault system characterized by south-dipping thrust faults. The décollement level is L1, occasionally L2.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento E-O inclinati verso sud. Il livello di scollamento è L1, più raramente L2.
Poggio Rusco - Ferrara thrust
Sovrascorrrimento Poggio Rusco - Ferrara
Poggio Rusco 2 thrust
Sovrascorrrimento Poggio Rusco 2
Poggio Rusco 3 thrust
Sovrascorrrimento Poggio Rusco 3
E-W trending thrust fault with an intermediate south dip. The décollement level is L1.
Sovrascorrimento ad andamento E-O mediamente inclinato verso sud. Il livello di scollamento è L1.
Poggio Rusco 4 thrust
Sovrascorrrimento Poggio Rusco 4
E-W trending thrust fault with an intermediate south dip. The décollement level is L2.
Sovrascorrimento ad andamento E-O mediamente inclinato verso sud. Il livello di scollamento è L2.
Correggio back-thrust
Retroscorrimento Correggio
NNE-SSW trending thrust fault with an intermediate WNW dip. The décollement level is L1.
Sovrascorrimento ad andamento NNE-SSO mediamente inclinato verso ONO. Il livello di scollamento è L1.
Bagnolo Fault System
Sistema di faglie Bagnolo
E-W trending fault system characterized by thrust and back-thrust. The décollement level is L1.
Sistema di faglie caratterizzato da sovrascorrimenti e retroscorrimenti ad andamento E-O. Il livello di scollamento è L1.
Bagnolo Thrust
Sovrascorrimento Bagnolo
E-W trending thrust fault with a steep south dip.
Sovrascorrimento ad andamento E-O molto inclinato verso sud.
Bagnolo back-thrust
Retroscorrimento Bagnolo
E-W trending thrust fault with a steep north dip. It is a back-thrust asscociated with the Bagnolo Thrust.
Sovrascorrimento ad andamento E-O molto inclinato verso nord. È un retroscorrimento associato al Sovrascorrimento Bagnolo.
Cavone Fault System
Sistema di faglie Cavone
E-W trending fault system characterized by thrust and back-thrust, and associated oblique slip faults. The décollement level is L1, occasionally L2.
Sistema di faglie caratterizzato da sovrascorrimenti e retroscorrimenti ad andamento E-O, e associate faglie oblique. Il livello di scollamento è L1, più rararmente L2.
Cavone outer splay Thrust
Sovrascorrimento secondario Cavone esterno
Cavone West minor 3 Back-thrust
Retroscorrimento Cavone minore ovest 3
E-W trending thrust fault with an intermediate north dip. The décollement level is L1. It is a back-thrust associated with the Cavone inner 1 Thrust.
Sovrascorrimento ad andamento E-O mediamente inclinato verso nord. Il livello di scollamento è L1. È un retroscorrimento associato con il Sovrascorrimento Cavone interno 1.
Cavone inner 1 Thrust
Sovrascorrimento Cavone interno 1
ENE-WSW trending thrust fault intermediate SSE-dipping. The décollement level is L1.
Sovrascorrimento ad andamento ENE-OSO mediamente inclinato verso SSE. Il livello di scollamento è L1.
Cavone inner 3 Thrust
Sovrascorrimento Cavone interno 3
Cavone minor 3 Back-thrust
Retroscorrimento Cavone minore 3
ENE-WSW trending thrust fault with a steep NNW dip. The décollement level is L1. It is a back-thrust associated with the Cavone inner 3 Thrust.
Sovrascorrimento ad andamento ENE-OSO molto inclinato verso NNO. Il livello di scollamento è L1. È un retroscorrimento associato con il Sovrascorrimento Cavone interno 3.
Cavone inner 4 Thrust
Sovrascorrimento Cavone interno 4
Cavone minor 4 Back-thrust
Retroscorrimento Cavone minore 4
E-W trending thrust fault with a steep north dip. The décollement level is L1. It is a back-thrust associated with the Cavone inner 4 Thrust.
Sovrascorrimento ad andamento E-O molto inclinato verso nord. Il livello di scollamento è L1. È un retroscorrimento associato con il Sovrascorrimento Cavone interno 4.
Cavone inner 5 Thrust
Sovrascorrimento Cavone interno 5
SE-NW trending thrust fault with an intermediate south-west dip. The décollement level is L1.
Sovrascorrimento ad andamento SE-NO mediamente inclinato verso SO. Il livello di scollamento è L1.
Cavone 1 Oblique slip fault
Faglia obliqua Cavone 1
NNE-SSW trending oblique slip vertical fault with WNW dip.
Faglia obliqua subverticale ad andamento NNE-SSO inclinata verso ONO.
Cavone East minor outer Thrust
Sovrascorrimento Cavone esterno minore est
SE-NW trending thrust fault with a steep south-west dip. The décollement level is L1.
Sovrascorrimento ad andamento SE-NO molto inclinato verso SO. Il livello di scollamento è L1.
Cavone 2 Oblique slip fault
Faglia obliqua Cavone 2
SSE-NNW trending oblique slip vertical fault with a ENE dip.
Faglia obliqua subverticale ad andamento SSE-NNO inclinata verso ENE.
Cavone East minor inner Thrust
Sovrascorrimento Cavone interno minore est
Cavone 3 Oblique slip fault
Faglia obliqua Cavone 3
SSE-NNW trending oblique slip fault with a steep WSW dip.
Faglia obliqua ad andamento SSE-NNO molto inclinata verso OSO.
Cavone East minor Back-thrust
Retroscorrimento Cavone minore est
ESE-WNW trending thrust fault with a steep NNE dip. The décollement level is L1. It is a back-thrust associated with the Cavone inner 5 Thrust.
Sovrascorrimento ad andamento ESE-ONO molto inclinato verso NNE. Il livello di scollamento è L1. È un retroscorrimento associato con il Sovrascorrimento Cavone interno 5.
Cavone 4 Oblique slip fault
Faglia obliqua Cavone 4
SE-NW trending oblique slip fault with a steep SW dip.
Faglia obliqua ad andamento SE-NO molto inclinata verso SO.
Cavone outer 1 Thrust
Sovrascorrimento Cavone esterno 1
Cavone West minor 1 Back-thrust
Retroscorrimento Cavone minore ovest 1
Cavone 5 Oblique slip fault
Faglia obliqua Cavone 5
Cavone outer 2 Thrust
Sovrascorrimento Cavone esterno 2
NE-SW trending thrust fault with an intermediate south-east dip. The décollement level is L1.
Sovrascorrimento ad andamento NE-SO mediamente inclinato verso SE. Il livello di scollamento è L1.
Cavone West minor 2 Back-thrust
Retroscorrimento Cavone minore ovest 2
Cavone minor 1 Back-thrust
Retroscorrimento Cavone minore 1
E-W trending thrust fault with a steep north dip. The décollement level is L1. It is a back-thrust associated with the Cavone inner 2 Thrust.
Sovrascorrimento ad andamento E-O molto inclinato verso nord. Il livello di scollamento è L1. È un retroscorrimento associato con il Sovrascorrimento Cavone interno 2.
Cavone inner 2 Thrust
Sovrascorrimento Cavone interno 2
Cavone minor 2 Back-thrust
Retroscorrimento Cavone minore 2
ENE-WSW trending thrust fault with a steep NNW dip. The décollement level is L1. It is a back-thrust associated with the Cavone inner 2 Thrust.
Sovrascorrimento ad andamento ENE-OSO molto inclinato verso NNO. Il livello di scollamento è L1. È un retroscorrimento associato con il Sovrascorrimento Cavone interno 2.
Novellara Fault System
Sistema di faglie Novellara
NE-SW trending fault system characterized by thrust and associated oblique slip faults. The décollement level is L1.
Sistema di faglie caratterizzato da sovrascorrimento ad andamento NE-SO e associate faglie oblique. Il livello di scollamento è L1.
Novellara Thrust
Sovrascorrimento Novellara
NE-SW trending thrust fault with an intermediate south-east dip.
Novellara 2 oblique slip fault
Faglia obliqua Novellara 2
Novellara 1 oblique slip fault
Faglia obliqua Novellara 1
Novellara 3 oblique slip fault
Faglia obliqua Novellara 3
SSE-NNW trending oblique slip fault with a steep ENE dip.
Faglia obliqua ad andamento SSE-NNO molto inclinata verso ENE.
Monferrato Front subdomain
Sottodominio Arco del Monferrato
The Monferrato front subdomain, one of the three parts composing the Northern Apennines thrust front, is characterized by thrust faults distributed in an arc-shaped geometry, with a mean E-W trend, mainly S-dipping. The activitiy ranges from Late Oligocene to Pleistocene
Il sottodominio del Fronte del Monferrato, uno dei tre settori che compongono il fronte dell'Appennino settentrionale,è caratterizzato da sovrascorrimenti disposti ad arco, con un andamento mediamente E-O, prevalentemente immergenti a sud. La loro attività è comresa tra l'Oligocene superiore e il Pleistocene.
Sali Vercellese Thrust
Sovrascorrimento Sali Vercellese
SE-NW trending thrust fault with an intermediate south-west dip.
Outer Monferrato thrust front
Fronte esterno dei sovrascorrimenti del Monferrato
ESE-WNW trending thrust fault with an intermediate SSW-dipping.
Montechiaro d'Asti Thrust
Sovrascorrimento Montechiaro d'Asti
Chivasso thrust
Sovrascorimmento Chivasso
Montecastello back- thrust
Retroscorrimento Montecastello
SE-NW trending thrust fault with a steep NE dip. It is a back-thrust associated with the Montecastello thrust.
Sovrascorrimento ad andamento SE-NO molto inclinato verso NE. È un retroscorrimento associato al Sovrascorrimento Montecastello.
Montecastello Thrust
Sovrascorrimento Montecastello
Inner Monferrato Thrust front
Fronte interno dei sovrascorrimenti del Monferrato
Tricerro Thrust
Sovrascorrimento Tricerro
Western Alps Back-thrusts subdomain
Sottodominio dei retroscorrimenti delle Alpi Occidentali
The Western Alps back-thrust subdomain is characterized by thrusts connected to the south-verging retrobelt of the Alps, active during Oligocene and Miocene. The thrusts and backthrusts have a ENE-WSW trend. They involve generally both the metamorphic basement and the Meso-Cenozoic sedimentary succession.
Il sottodominio dei retroscorrimenti delle Alpi Occidentali è caratterizzato da sovrascorrimenti connessi alla porzione di catena Alpina con vergenza verso sud, attiva durante l'Oligocene e il Miocene. I sovrascorrimenti e retroscorrimenti hanno un andamento ENE-OSO. Essi coinvolgono generalmente sia il basamento metamorfico che la successione sedimentaria meso-cenozoica.
Salussola Fault System
Sistema di faglie Salussola
ENE-WSW trending fault system characterized by NNW-dipping thrust faults. They involve both the metamorphic basement and the Mesozoic sedimentary succession. The activity is dated Upper Eocene-Upper Oligocene.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento ENE-OSO e immersione verso NNO. I sovrascorrimenti coinvolgono sia il basamento metamorfico che la successione sedimentaria mesozoica. L'attività è riferibile all'Eocene superiore-Oligocene superiore.
Salussola 1 Thrust
Sovrascorrimento Salussola 1
ENE-WSW trending thrust fault with a gentle NNW dip.
Sovrascorrimento ad andamento ENE-OSO debolmente inclinato verso NNO.
Salussola Thrust
Sovrascorrimento Salussola
Ghemme - Borgoticino Fault System
Sistema di faglie Ghemme - Borgoticino
NE-SW trending fault system characterized by thrusts and back-thrusts, active in the Lower-Middle Miocene. They involve basement and sedimentary succession up to Middle Miocene.
Sistema di faglie ad andamento NE-SO caratterizzato da sovrascorrimenti e retroscorrimenti attivi nel Miocene inferiore-medio. Essi coinvolgono sia il basamento metamorfico che la successione sedimentaria fino al Miocene medio.
Sesia Thrust
Sovrascorrimento Sesia
NE-SW trending thrust fault with a steep NW dip.
Sovrascorrimento ad andamento NE-SO molto inclinato verso NO.
Sesia Back-thrust
Retroscorrimento Sesia
ENE-WSW trending thrust fault with a gentle SSE dip. It is a back-thrust associated with Sesia Thrust.
Sovrascorrimento ad andamento ENE-OSO debolmente inclinato verso SSE; è un retroscorrimento associato con il Sovrascorrimento Sesia.
Romentino Fault System
Sistema di faglie Romentino
ENE-WSW trending thrust faults, NNW dipping, with décollement at the level of the Eocene terrigenous succession. The activity is dated Lower-Middle Miocene.
Sistema di faglie caratterizzato da sovrascorrimenti ad andamento ENE-OSO e immersione verso NNO, con livello di scollamento nella successione terrigena eocenica. L'attività è riferibile al Miocene inferiore-medio.
Turbigo Thrust
Sovrascorrimento Turbigo
ENE-WSW trending thrust fault with intermediate NNW dip.
Sovrascorrimento ad andamento ENE-OSO mediamente inclinato verso NNO.
Romentino Thrust
Sovrascorrimento Romentino Sud
Campidano Graben Domain
Dominio del Graben del Campidano
The Campidano Graben domain corresponds to a NW-SE elongated Plio-Quaternary depression lies on the SW sector of the Sardinia block and extends from the Gulf of Oristano to the NW and the Gulf of Cagliari to the South. The graben is probably related to the coeval extension in the Tyrrhenian Sea; it is in part superimposed on the Oligo-Miocene rift system and involves mostly reactivated normal faults (Casula et al., 2001; Carmignani et al., 2001; 2015). This domain is characterized by prevalently NW-SE striking normal faults organized in half-graben geometry. In the central and southern sectors of the basin two main longitudinal master faults (i.e.: Isili fault, and Monastir fault) are along the eastern side. Several associated second order synthetic and antithetic structures are present in the subsurface of the Campidano basin. In the same way, minor extensional tectonic features related to the Plio-Quaternary extensional phase have been also mapped affecting the Variscan basement out of the borders of the Campidano valley.
Il dominio del Graben del Campidano corrisponde con una depressione plio-quaternaria allungata NO-SE, ubicata nel settore SO del blocco sardo, e si estende dal Golfo di Oristano, a nord-ovest, fino al Golfo di Cagliari, a sud. Il graben è probabilmente legato alla coeva estensione nel Mar Tirreno, è sovraimposto in parte al sistema di rift dell'Oligo-Miocene e coinvolge prevalentemente faglie normali riattivate (Casula et al., 2001; Carmignani et al., 2001; 2015). Il dominio è caratterizzato da faglie normali prevalentemente a direzione NO-SE organizzate con geometria ad half-graben. Nei settori centrale e meridionale del bacino, due faglie principali longitudinali (faglia di Isili e la faglia di Monastir) bordano il lato orientale. Diverse strutture di secondo ordine associate, sintetiche e antitetiche, sono presenti nel sottosuolo del bacino. Inoltre, elementi estensionali minori, connessi con la fase estensionale plio-quaternaria, sono stati mappati fuori dal bacino del Campidano, a coinvolgere il basamento varisico.
Sicilian-Maghrebian Domain
Dominio Sicilide-Magrebide
The Sicilian-Maghrebian domain extends in the whole Sicily west of the Etna volcano and the Calabro- Peloritane Units and north of the Catania-Gela Foredeep. This structural domain is related to the complex Sicilian Fold and Thrust Belt system deriving from the Miocene-Pliocene deformation of the Northern African Continental Margin. On the whole, the domain is characterized by prevalently E-W trending, S- and locally SE-verging thrust tectonic related structures that show variable shortening and rotational rates. Compressive structures are locally dislocated by strike-slip faults mainly related to the rotational Plio-Pleistocene phase. High-angle normal fault systems related to early Pliocene-Present extensional tectonics are also present.
Il Dominio Sicilide-Magrebide si estende su tutta la Sicilia, a ovest dell'Etna e delle unità Calabro-Peloritane, e a nord dell'avanfossa Gela-Catania. Questo dominio strutturale è connesso al complesso sistema a pieghe e sovrascorrimenti (Sicilian Fold and Thrust Belt system) derivante dalle deformazioni mio-plioceniche del margine continentale africano. Nell'insieme, il dominio è caratterizzato da sovrascorrimenti ad andamento prevalentemente E-O vergenti a S e, localmente, a SE con tassi di raccorciamento e rotazione variabili. Le strutture compressive sono localmente dislocate da faglie trascorrenti prevalentemente connesse a rotazione durante il Plio-Pleistocene. Sono presenti anche sistemi di faglie normali ad alto angolo connesse alla tettonica estensionale del Pliocene inferiore-attuale.
Northern Apennines Domain
Dominio Appennino Settentrionale
The Northern Apennines domain is characterized by thrust fault imbricated structures, mainly E-vergent, related to the Apenninic orogenic phase (post-collisional neoalpine) active from Chattian. Several decollemenet low-competence levels are recognized (the deeper at the top of the Triassic Anidriti di Burano, the shallower located on Lower Jurassic Rosso Ammonitico, Lower Cretaceous Marne a Fucoidi, Eocene-Lower Miocene Scaglia cinerea or Messinian Evaporites). Back-thrusts are associated to the main structures. The boundary between Northern and Southern Apennines domains is the Ortona-Roccamonfina lineament.
Il dominio dell'Appennino Settentrionale è caratterizzato da sovrascorrimenti, prevalentemente vergenti a est, legati alla fase orogenica Appenninica (post-collisionale, neoalpina) attiva dal Cattiano. Sono riconosciuti diversi livelli di scollamento a bassa competenza (il più profondo al tetto delle Anidriti di Burano triassiche, i più superficiali posti variabilmente al Rosso Ammonitico del Giurassico inferiore, alle Marne a Fucoidi del Cretacico inferiore, alla Scaglia cinerea dell'Eocene-Miocene inferiore o alle evaporiti del Messiniano). Retroscorrimenti sono associati alle strutture principali. Il limite tra i domini dell'Appennino Settentrionale e Meridionale è posto in corrispondenza della linea Ortona-Roccamonfina.
Sardinia Variscan basement Domain
Dominio del basamento Ercinico della Sardegna
The largest part of Sardinia consists of a Variscan basement, composed by different tectonic units deformed and emplaced with a tectonic transport direction toward SW during the Early Carboniferous and of a Permo-Carboniferous batholith emplaced between 340 and 280 Ma (Carmignani et al., 2001). The main tectonic features are ductile and brittle-ductile overthrusts developed during the continental collision between Gondwana and the Armorica Terranes Assemblage. Low- to high-angle normal faults developed during collapse of the thickened crust in the final stages of the Variscan orogeny, in part during emplacement of the plutonic complex, the dyke complex and development of a volcano-sedimentary complex of Upper Carboniferous–Lower Triassic age (Carmignani et al., 2015). The External zone, cropping out in the SW sector (Iglesiente and Sulcis), is the less metamorphosed and deformed portion of the Sardinia Variscan chain allowing to distinguish fold and thrust (Carmignani et al., 2004). The Variscan tectonic structures are locally cut or reactivated by the most recent normal faults related to the extensional phase responsible for the Oligocene-Miocene Sardinia Rifting System.
La maggior parte della sardegna è costituita da basamento varisico, composto da differenti unità tettoniche, deformate e messe in posto, con una direzione di trasporto verso SO, durante il Carbonifero inferiore. A queste unità si aggiunge un batolite permo-carbonifero messo in posso tra 340 e 280 Ma (Carmignani et al., 2001). I principali elementi tettonici sono overthrust duttili e fragili-duttili sviluppatisi durante la collisione tra terranes di provenienza gondwanica e armoricana. Faglie normali, da basso ad alto angolo, si sono sviluppate durante il collasso di crosta inspessita, nelle fasi finali dell'orogenesi varisica, e in parte durante la messa in posto del complesso plutonico, dei dicchi e lo sviluppo del complesso vulcano-sedimentario (Carbonifero superiore–Triassico inferiore) (Carmignani et al., 2015). La Zona Esterna, affiorante nel settore SO (Iglesiente e Sulcis), è la meno metamorfosata e deformata della catena varisica, consentendo di distinguere pieghe e sovrascorrimenti (Carmignani et al., 2004). Le strutture tettoniche varisiche sono localmente tagliate o riattivate da faglie normali più recenti connesse con la fase estensionale responsabile della formazione del sistema di rifting della Sardegna (Oligocene-Miocene).
Apennines extensional Domain
Dominio estensionale appenninico
The domain is characterized by normal faults, mainly NW-SE and NNW-SSE oriented, related to the extensional regime active from the Middle-Upper Miocene due to the counter-clockwise rotation of the Corsica-Sardinia block, the opening of Tyrrhenian Sea, the foreland flexural process, and the fast overall uplift of the Apennines chain. The age of inception rejuvenates from west to east superimposing on the compressional phases. In the Northern Apennines extensional kinematic is associated with minor transtensional, with master faults are often E-dipping with antithetic W-dipping faults; in the Southern Apennines both right- and left-strike-slip faults are observed, related to counter- and clockwise rotation respectively.
Il dominio estensionale appenninico è caratterizzato da faglie normali, ad andamento prevalente NO-SE e NNO-SSE, connesse al regime estensionale attivo dal Miocene medio-superiore connesso alla rotazione antioraria del blocco sardo-corso, all'apertura del mar Tirreno, ai processi di flessurazione dell'avampaese, e al generale sollevamento della catena appenninica. L'età di inizio del regime estensionale ringiovanisce da ovest verso est sovraimponendosi alle fasi compressive. Nell'Appennino Settenrionale la cinematica estensionale è associata a transtensione secondaria, con faglie principali generalmente immergenti a E e faglie antitetiche immergenti a O. Nell'Appennino Meridionale sono riconosciute sia faglie trascorrenti sinistre che destre, connesse, a rotazione oraria e antioraria, rispettivamente.
Passo Cattivo fault
Quarto San Lorenzo fault
Fossa fault
Molina Aterno fault
Costa Castello fault
Fontechio fault
Colle Cocurello fault
Vettore 5 fault
Colle Praticciolo fault
Vettoretto 2
Civitaretenga fault
Vettore 1
Colle Cicogna fault
Vettore 3 fault
Barisciano fault
Strada Frontignano - M Cornaccione fault
Bazzano fault
Valle delle Fonti fault
Scoglio della Volpe - Colle Abieri fault
Strada Frontignano - Cornaccione 2 fault
Forca di Presta fault
Acciano fault
Passo Cattivo 3 fault
Monte Porche fault
Palazzo Borghese fault
Monte Cornaccione - Le Pianelle
Monte Cornaccione fault
Monte Argentella fault
Monte Bicco fault
Monte Abuzzago 1 fault
Frontignano fault
Colle Infante fault
Cordone del Vettore fault
Base Monte Vettore fault
Colle Infante - Monte Rotondo fault
Base Monte Vettore 2 fault
Base Monte Vettore 3 fault
Vigne Basse fault
Villa S.Angelo fault
Valle Bovacchio fault
Vallecupa fault
Vettoretto fault
Vettoretto 3
San Rocco fault
San Martino fault
San Pio delle Camere fault
San Demetrio 3 fault
San Demetrio fault
Poggio Picenze fault
Ripa fault
Monticchio fault
Paganica fault
Sardinia Graben system Domain
Dominio del sistema dei graben della Sardegna
The Sardinia Graben System characterizes the western sector of the Sardinia block with a roughly N-S elongated depression running from the Gulf of Asinara to the North and the Gulf of Cagliari to the south (Carmignani et al., 2001; 2015). The system started developing since the Oligocene up to Miocene upon the Variscan metamorphic and plutonic basement as a result of the extensional regime that affected the Iberian-Europe Region at about 34 Ma (Casula et al., 2001). The present-day structure of the Sardinia Graben System consists of large graben whose margins are well exposed and bordered by major N-S striking normal faults with associated minor parallel and transverse structures (Casula et al., 2001; Carmignani et al., 2015).
Il sistema dei graben della Sardegna, che caratterizza la porzione occidentale del blocco sardo, si presenta come una depressione con un andamento allungato circa N-S, dal Golfo dell'Asinara, a nord, al Golfo di Cagliari, a sud (Carmignani et al., 2001; 2015). I graben hanno iniziato a svilupparsi a partire dall'Oligocenefino al Miocene, sul basamento metamorfico e plutonico varisico, come risultato del regime estensionale che ha coinvolto la regione iberico-europea a partire da 34 Ma (Casula et al., 2001). L'attuale assetto del sistema dei graben della Sardegna consiste in ampi graben i cui margini, ben esposti, sono bordati da faglie normali principali ad andamento N-S, con associate faglie minori parallele e strutture trasversali (Casula et al., 2001; Carmignani et al., 2015).
Sestri-Voltaggio Lineament
Linea Sestri-Voltaggio
The Sestri-Voltaggio lineament is a N-S lineament acting as boundary between Alps and Apennines chains with opposite vergence, it was active, as transform fault (Scholle, 1970), during the eo- and meso-alpine tectonic phases
La linea Sestri-Voltaggio, lineamento ad andamento N-S che ha agito come limite tra le catene alpina e appenninica caratterizzate da opposte vergenze, è stato attivo come faglia trasforme (Scholle, 1970) durante le fasi tettoniche eo- e meso-alpina.
Taormina Line
Linea di Taormina
The Taormina Line identifies the southern border of the Calabride-Peloritane domain. This Tectonic Line is interpreted to be a NNE dipping thrust fault (Bonardi et al., 2001).
La Linea di Taormina identifica il bordo meridioanle del Dominio Calabro-Peloritano. Questa linea è interpretata come un sovrascorrimento immergente a NNE (Bonardi et al., 2001).
Ligurian Fault Domain
Dominio Ligure
The Ligurian domain is characterized by thrusts active during the collisional mesoalpine underthrusting and underplating (Late Cretaceous-Middle Eocene); furtherly active during post-collisional neoalpine eastward overthrusting (Oligocene-early Pliocene or Pleistocene - Sillaro e Marecchia). Both ductile and fragile deformations are recorded.
Il Dominio Ligure è caratterizzato da sovrascorrimenti attivi durante la fase collisionale mesoalpina (underthrusting e underplating; Cretacico superiore-Eocene medio); successivamente attivi durante la migrazione verso est connessa alla fase post-collisionale neoalpina (Oligocene-Pliocene inferiore e Pleistocene - zona del Sillaro e Marecchia). Sono registrate sia deformazioni duttili che fragili.
Calabride-Peloritane Domain
Dominio Calabro-Peloritano
The Calabride-Peloritane domain is a fault-bounded exotic terrane located at the intersection between the NW-SE-trending Southern Apennines and the E-W-trending Sicilian Maghrebides, characterized by: i) pre-Mesozoic crystalline basement with ductile deformations (Hercynian Orogeny), ii) Alpine (Apennines) Oligo-Miocene reverse faults (Bonardi et al., 2001) associated with shear zones, and iii) post-orogenic extensional, sub-vertical and sub-parallel N-S, NE-SW, and NW-SE, with minor NNE-SSW and E-W, normal faults (upper Miocene and upper Pleistocene-Holocene). At its N and S margins, the Calabride-Peloritane domain is bounded by the Sangineto and Taormina lines.
Il dominio Calabro-Peloritano è un terrane esotico bordato da faglie e posizionato all'intersezione tra l'Appennino Meridionale, ad andamento NO-SE, e quello Sicilide-Magrebide ad andamento E-O. Il dominio è caratterizzato da: i) un basamento cristallino pre-mesozoico con deformazioni duttili (Orogenesi Ercinica), ii) faglie inverse appenniniche dell'Oligo-Miocene (Bonardi et al., 2001) con associate zone di taglio, e iii) faglie normali post-orogeniche, sub-verticali e sub-parallele, ad andamento N-S, NE-SO, e NO-SE, e secondariamente NNE-SSO e E-O (Miocene superiore e Pleistocene superiore-Olocene). Il Dominio Calabro-Peloritano è bordato a nord e sud, rispettivamente, dalla Linea di Sangineto e dalla Linea Taormina.
Penninic Domain
Dominio Pennidico
The Penninic domain, part of the Alpine chain, groups the continental and oceanic nappes which issued from the distal European continental margin and Mesozoic ocean, characterized by ductile deformations and Europe-vergent thrust faults, bounding the tectonic windows or separating units, mainly stacked during Paleogene. The domain is marked by a severe Alpine metamorphic overprint with the exception of pre-Alpine klippen.
Il dominio Pennidico, parte della catena alpina, raggruppa falde costituite da unità delle porzioni distali del margine continentale europeo e dell'oceano antistante. Le falde sono caratterizzate da deformazioni duttili e da sovrascorrimenti con vergenza europea, che costituiscono i limiti di finestre tettoniche o di unità tettoniche, prevalentemente impilate durante il Paleogene. Il dominio, con l'eccezione di klippen pre-alpini, è marcato da una forte sovraimpronta metamorfica.
Austroalpine Domain
Dominio Austroalpino
The Austroalpine domain, descending from the Africa ocean-facing continental margin, overlies the Penninic domain, as part of the Alpine chain. The faults are boundaries of the main nappes and tectonic windows showing the Penninic domain units. The activity is dated to pre-Late Cretaceous (pre-collisional phase, eoalpine) for the eastern part and to Late Cretaceous-Eocene (collisional, mesoalpine) for the western part.
Il dominio Austroalpino, parte della catena alpina e derivante dal margine continentale africano prossimo all'oceano, ricopre il dominio Pennidico. Le faglie sono i limite delle falde principali e delle finestre tettoniche che mostrano le unità del dominio Pennidico sottostante. L'attività è riferibile alla parte iniziale del Cretacico superiore (fase pre-collisionale, eoalpina) nel settore orientale, e al Cretacico superiore-eocene (fase collisionale, mesoalpina) nel settore occidentale.
fault (IT-0049)
Jaufen-Passeier Fault System
Southalpine Domain
Dominio Sudalpino
The Southalpine domain, as part of the Alpine chain, is characterized by large scale thrusting and folding, mainly E-W and NE-SW trending, with dominant vergence toward south. In addition, extensional faults, antithetic and syntethic mainly NW-SE trending, related to Upper Triassic-Middle Jurassic rifting are preserved within large inverted compressional structures. Some areas still preserve the record of Variscan/Hercynian deformations with limited metamorphic overprint. The compressional activity (post-collisional, neoalpine) started during the Tertiary (Oligocene) and progressively propagated towards the foreland; in the western sector evidences of Cretaceous compressional phases are known. The northern boundary of this domain is represented by the Insubric Fault System.
Il dominio Sudalpino, parte della catena alpina, è caratterizzato da sovrascorrimenti e piegamenti a scala regionale, prevalentemente ad andamento E-O e NE-SO, con vergenza dominante verso sud. Sono inoltre preservate faglie dirette, sintetiche e antitetiche, prevalentemente ad andamento NO-SE, connesse al rifting del Triassico superiore-Giurassico medio, preservate dalle strutture compressive. In alcune aree sono ancora presenti elementi delle deformazioni Varisiche (erciniche) con limitata sovraimpronta metamorfica. L'attività compressiva (post-collisionale, neoalpina) è iniziata durante il Terziario (Oligocene) e progressivamente si è propagata verso l'avampaese; nel settore occidentale sono note evidenze di attività compressiva cretacica. Il limite settentrionale del dominio è rappresentato dal sistema di faglie della Linea Insubrica.
Sangineto Line
Linea di Sangineto
The Sangineto Line marks the northern border of the Calabride-Peloritane domain. T the Sangineto line seems to be a complex fault system with a left-lateral strike-slip component (Bonardi et al., 2001).
La Linea di Sangineto marca il bordo settentrionale del Dominio Calabro-Peloritano. Essa si presenta come un complesso sistema di faglie con una componente trascorrente sinistra (Bonardi et al., 2001).
Hyblean foreland Domain
Avampaese Ibleo
The Hyblean foreland is characterized by sub-parallel normal faults, mainly NE-SW oriented and NW dipping, related to the Mesozoic extensional phase (Patacca et al., 1979; Lentini et al., 1987) and to a Plio-Quaternary collapse as response to the migration of the thrust front. In addition, Plio-Pleistocene NW-SE oriented normal faults and NNE-SSW strike-slip faults, with dextral movement, occur (Ghisetti & Vezzani, 1981; Lentini et al., 1984).
L'avampaese Ibleo è caratterizzato da faglie normali sub-parallele, prevalentemente orientate NE-SO e immergenti a NO, connesse alla fase estensionale mesozoica (Patacca et al., 1979; Lentini et al., 1987) e al collasso plio-quaternario, come risposta alla migrazione del fronte dei sovrascorrimenti. Inoltre, sono presenti faglie normali plio-pleistoceniche orientate NO-SE e faglie trascorrenti destre a orientazione NNE-SSO (Ghisetti & Vezzani, 1981; Lentini et al., 1984).
﻿Hyblean - Malta Escarpment_09
Scarpata di Malta_09
﻿Hyblean - Malta Escarpment_02
Scarpata di Malta_02
Helvetic Domain
Dominio Elvetico
The Helvetic domain, part of the Alpine chain, is characterized by Europe-vergent (N and NW) nappes derived from the proximal part of the European continental margin, imbricated from the Oligocene onwards.
Il dominio Elvetico, parte della catena alpina, è caratterizzato da una vergenza europea (N e NO) delle falde derivanti dalle porzioni prossimali del margine continentale europeo, impilate a partire dall'Oligocene.
Apulia foreland Domain
Avampaese Apulo
The Apulia foreland domain represents the outcropping portion of the Southern Apennines foreland. This structural domain is characterized by NW-SE striking normal faults linked to the early Middle Pleistocene flexural tectonics and to the following Middle–Upper Pleistocene extensional tectonics. These faults affected mainly the foreland buried below the front of the chain and below the foredeep deposits. The outcropping Apulia sector (Apulia foreland) exhibits a regional pattern of large scale deformation which is manifested through a system of NW-SE extensional structures affecting both its smoothly flexure along the contact with the Bradanic foredeep and its eastern sector; locally minor striking NE-SW normal faults are also present. The northern border of this structural Domain is marked by the E-W trending Mattinata fault and in general by the Gargano Fault System.
Il dominio dell'Avampaese Apulo rappresenta la porzione affiorante dell'avampaese dell'Appennino Meridionale. Questo dominio strutturale è caratterizzato da faglie normali a direzione NO-SE connesse alla flessurazione dell'inizio del Pleistocene medio e alla seguente tettonica estensionale del Pleistocene medio-superiore. Queste faglie coinvolgono prevalentemente l'avampaese sepolto sotto il fronte della catena e dai depositi di avanfossa. Il settore affiorante mostra un reticolo di deformazioni a larga scala manifestate da un sistema di strutture estensionali NO-SE che coinvolgono sia la zona interna, al margine della Fossa Bradanica, sia il settore orientale; localmente sono presenti faglie normali minori a direzione NE-SO. Il bordo settentrionale di questo dominio strutturale è marcato dalla faglia di Mattinata, ad andamento E-O, e in generale dal Sistema di faglie Gargano.
Gargano Fault System
Sistema di faglie del Gargano
The Gargano Fault System characterizes the Gargano Promontory, that represents the northern portion of the Apulian foreland emerging from the Adriatic Sea. The promontory shows E-W elongated anticline morphology and it is affected by NW-SE and E-W trending main faults and by NE-SW trending minor faults. The major structure is the E-W trending, south dipping, Mattinata Fault cutting cross the southern border of the Gargano Promontory (Funiciello et al., 1988). Many Authors suggest that the Gargano faults might have experienced different activity and different sense of motion in different tectonic regimes and they propose a multi-phase kinematics (Patacca & Sacandone, 2004 and references therein). Major evidences are in favour for a dextral strike slip kinematics along the Mattinata Fault from Late Pliocene to the present (Piccardi, et al., 2004).
Il sistema di faglie del Gargano caratterzza il promontorio del Gargano, che rappresenta la porzione settentrionale dell'avampaese Apulo. Il promontorio è caratterizzato da un'anticlinale allungata in direzione E-O, interessata da faglie principali ad andamento NO-SE ed E-O, e da faglie minori NE-SO. La struttura maggiore, denominata faglia di Mattinata, ha andamento E-O immergente verso sud, e taglia il borso meridionale del promontorio del Gargano (Funiciello et al., 1988). Diversi autori hanno ipotizzato che le faglie del sistema siano state interessate da diverse fasi di attività e da differente tipo di movimento, in diversi regimi tettonici; essi hanno proposto una cinematica multifase (Patacca & Sacandone, 2004 e bibliografia associata). Le maggiori eveidenze sono a favore di cinematica trascorrente destra per la faglia di Mattinata a partire dal Pliocene superiore fino ad oggi (Piccardi, et al., 2004).
Etna volcano Domain
Dominio dell'Etna
The Etna volcano, in eastern Sicily, is the largest and most active stratovolcano in Europe. Its eruptive activity started during the middle Pleistocene on the structural domain of the Gela– Catania Foredeep in the front of the the Apennine–-Maghrebian thrust belt at the intersection of two active regional master faults, the Hyblean–Malta Escarpment and the Messina–Fiumefreddo line (Branca et al., 2011). The Etna structural setting represents the result of the interaction of regional tectonics, volcano-tectonic processes and local scale volcano-related and gravitative processes (Lo Giudice et al., 1982). The northern termination of the Malta Escarpment dissects the base of the eastern flank of Etna volcano through a set of NNW–SSE normal faults called Timpe fault system (Lo Giudice et al. 1982). The most active faults in this system are the Moscarello, San Leonardello and Acireale faults. The E-W trending Pernicana-Fiumefreddo fault system and the NW-SE trending Tremestieri and Trecastagni faults represent the northern and the southern border of a sliding sector. Both these faults systems are characterized by seismic and aseismic (creep) activity.
L'Etna, nella Sicilia orientale, è il più grande e attivo strato-vulcano in Europa. La sua attività eruttiva è iniziata durante il Pleistocene medio sul dominio dell'Avanfossa Gela-Catania, di fronte alla catena Appenninico-Magrebide e all'intersezione di due faglie attive di importanza regionale, la Scarpata Ibleo-Maltese e la linea Messina-Fiumefreddo (Branca et al., 2011). L'assetto strutturale dell'Etna è il risultato dell'interazione della tettonica regionale, dei processi vulcano-tettonici e di processi locali connessi al vulcano e alla gravità (Lo Giudice et al., 1982). La terminazione settentrionale della Scarpata Ibleo-Maltese taglia la base del fianco orientale del vulcano attraverso una serie di faglie normali, ad andamento NNO-SSE, chiamate Sistema delle Timpe (Lo Giudice et al. 1982). La faglie più attive del sistema sono Moscarello, San Leonardello e Acireale. Il Sistema Pernicana-Fiumefreddo, ad andamento E-O, e le faglie Tremestieri eTrecastagni, ad andamento NO-SE, rappresentano i bordi settentrionale e meridionale di un settore in scivolamento. Entrambi questi sistemi sono caratterizzati da attività sismica e asismica (creep).
Nicolosi fault
Santa Tecla fault
Pernicana fault
Massa Annunziata fault
Santa Tecla - Linera fault
Moscarello fault
Santa Tecla - Santa Venerina fault
Guzzi fault
Sant'Alfio fault
Macchia - Stazzo fault
Santa Maria la Scala fault
Guardia fault
San Giovanni Bosco fault
Tremestieri fault
Gurna fault
San Leonardello fault
Pernicana_16 fault
Santa Venera_02 fault
Acireale fault
Provenzana fault
Trecastagni fault
Santa Venera fault
Pernicana_05 fault
Santa Venera_01 fault
Catania-Gela foredeep Domain
Avanfossa Catania-Gela
The Catania-Gela Foredeep domain extends between the front of the Apenninic-Maghrebides Belt and the Hyblean Plateau (foreland). The depression starts developing in the Late Pliocene from the inflection of the carbonate substrate related also to the frontal nappe loading (Catalano et al., 1993). The north-western sector the Catania-Gela Foredeep is fully occupied by the allochthonous units of the frontal wedge of the chain, the Gela Nappe, of which the S and SE verging front represents the main structural feature. A system of NE-SW trending normal faults identifies its south-eastern border and the separation with the Hyblean Foreland domain, partially flexured below the foredeep. Minor extensional elements mainly NE-SW striking locally deform the Upper Pliocene-Pleistocene sedimentary succession.
Il Dominio di avanfossa Catania-Gela si estende tra il fronte della catena Appenninico-Magrebide e il Plateau Ibleo (avampaese). Lo sviluppo della depressione è iniziato nel Pliocene superiore, a partire dall'inflessione del substrato carbonatico connessa anche al carico delle falde frontali (Catalano et al., 1993). Il settore nord-occidentale dell'avanfossa Catania-Gela è completamente occupato da unità alloctone del cuneo frontale della catena (Falda di Gela) le cui strutture principali sono S- e SE-vergenti. Un sistema di faglie normali a direzione NE-SO identifica il suo bordo sudorientale e la separazione con il dominio dell'Avampaese Ibleo, parzialmente flessurato sotto l'avanfossa. Elementi estensionali minori, prevalentemente a direzione NE-SO, deformano la successione sedimentaria del Pliocene superiore-Pleistocene.
Southern Apennines Domain
Dominio Appennino meridionale
The Southern Apennines Domain developed through the deformation of the thinned oceanic-transitional to continental crust of the Liguria-Piedmont Ocean and the Africa continental passive margin, starting in the Late Cretaceous. The accretion of the fold-and-thrust belt is strictly linked to the continental collision and post-collisional activity, ranging from late Oligocene to early Pleistocene, with eastward migration of the deformation and piling and out-of-sequence thrusting. The Southern Apennine mountain chain is formed by a deep-seated carbonate duplex system tectonically overlain by a thick pile of NE-verging rootless nappes derived from basin and platform domains (Patacca & Scandone, 2007). Each tectonic-sedimentary unit (nappe) is bordered by major thrusts or, more frequently, by a group of thrusts. The internal nappe geometry is complicated by second order of folds and thrusts mainly NE-verging. In addition, some allochthonous unit, locally placed up as gravitative flows, constitute the easternmost and more advanced thrust sheets outcropping in the Southern Apennines.This complex NE-verging thrust belt developed during Neogene and Quaternary times along the eastward-retreating west-directed subduction of the Apulo-Adriatic lithosphere (Scrocca, 2010 ).
Il Dominio Appennino Meridionale si è sviluppato attraverso la deformazione di crosta assottigliata oceanica e di transizione dell'Oceano Ligure-Piemontese e del margine continentale passivo africano, a partire dal Cretacico superiore. L'accrezione della catena a pieghe e sovrascorrimenti è strettamente connessa alla collisione continentale e alle fasi post-collisionali, nell'intervallo Oligocene superiore - Pleistocene inferiore, con migrazione verso est della deformazione e dell'impilamento, con sovrascorrimenti fuori sequenza. La catena dell'Appennino Meridionale è formata da un sistema radicato nei carbonati e raddoppiato, tettonicamente sovrascorso da una potente pila di falde scollate, NE vergenti, derivate da domini di bacino e piattaforma (Patacca & Scandone, 2007). Ciascuna unità tettono-sedimentaria (falda) è bordata da sovrascorrimenti principali o, più frequentemente, da più sovrascorrimenti. La geometria interna delle falde è complicata da pieghe e sovrascorrimenti di secondo ordine, prevalentemente vergenti a NE. Inoltre, alcune unità alloctone, localemente messe in posto come colate gravitative, costituiscono gli elementi più orientali ed esterni affiornati nell'Appennino Meridionale. Questa complessa catena NE vergente si è sviluppata durante il Neogene e il Quaternario lungo la zona di subduzione della litosfera Apulo-Adriatica in arretramento verso est (Scrocca, 2010 ).
Bradanic Trough Domain
Fossa Bradanica
The Bradanic Trough represents the Pliocene-present-day southern Apennines foredeep. It is a NW-SE elongated foreland basin separating the Apennine chain from the Apulia foreland. This flexural depression developed at the front of the Apennine thrust belt and have been filled by Pliocene-Pleistocene deposits. This domain is mainly characterized by the presence of NW-SE trending E-verging thrusts due to the involvement in the Apennines thrust front deformation or to the Apennine blind thrust propagation. At same time, syn-depositional extensional structures are present as a results of the propagation of the deep extensional tectonic pattern affecting the buried foreland
La Fossa Bradanica rappresenta l'avanfossa dell'Appennino Meridionale a partire dal Pliocene fino a oggi. Si tratta di un bacino allungato NO-SE, che separa la catena appenninica dall'avampaese Apulo. Questa depressione flessurale si è sviluppata al fronte della catena ed è stata colmata da sedimenti plio-pleistocenici. Il dominio è caratterizzato prevalentemente da sovrascorrimenti ad andamento NO-SE, E vergenti, connessi all'avanzata del fronte della catena o alla propagazione di sovrascorrimenti ciechi. Allo stesso tempo, sono presenti strutture estensionali sindeposizionali risultato della propagazione di strutture estensionali profonde e sepolte che coinvolgono l'avampaese.
All named tectonic boundary objects that are located (at least partly) in Poland, are identified by an ID with the prefix „PL“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in Poland displayed on the European HIKE fault database.
Granice tektoniczne w Polsce
Tectonic Boundary in Poland
Inner Carpathians
Inner Carpathians are constituted by the cristalline basement and overthrusted sedimentary nappes of the Tatras, Podhale flysh basin and the Pieniny Klippen Belt.
Karpaty wewnętrze obejmują krystaliczne podłoże I fałdowo-płaszczowinową pokrywę osadową Tatr, fliszowe Podhale oraz Pieniński Pas Skałkowy.
Karpaty wewnętrzne
Podhale synclinorium
Palaeogene flysh basin in front of the Tatra Mountains, overlying ALCAPA basement.
Fliszowy basen przedgórski Tatr, rozwinięty na mikropłycie ALCAPA.
Synklinorium podhalańskie
Białka fault
The system of discrete faults in the dextral strike-slip fault zone. Probably deeply rooted and reactivated in the Miocene. In morphology forming the Białka river valley. Method of observation: surface observation, geological mapping. (Country Report fault code: F-3)
System uskoków w strefie uskoku prawoprzesuwczego. Prawdopodobnie zakorzeniony głęboko i reaktywowany w miocenie. W morfologii wykorzystany przez dolinę Białki. Metody obserwacji: odsłonięcia, kartowanie geologiczne. (Kod uskoku w Raporcie krajowym projektu HIKE: F-3)
Uskok Białki
Biały Dunajec fault zone
The system of discrete faults in the sinistral strike-slip fault zone. Probably deeply rooted and reactivated in the Miocene. In morphology forming the Biały Dunajec river valley. Method of observation: surface observation, geological mapping. (Country Report fault code: F-2)
System uskoków w strefie uskoku lewoprzesuwczego. Prawdopodobnie zakorzeniony głęboko w podłożu i reaktywowany w miocenie. W morfologii wykorzystany przez dolinę Białego Dunajca. Metody obserwacji: odsłonięcia, kartowanie geologiczne. (Kod uskoku w Raporcie krajowym projektu HIKE: F-2)
Strefa uskokowa Białego Dunajca
Pieniny Klippen Belt
A major suture zone coming from the Alps all along the Carpathian chain, forming the boundary between ALCAPA, to the S, and the Eurasian plate, to the N. Created during ALCAPA accretion in the Neogene. Perfectly recognized by geological mapping and recorded by geophysical methods. Recent seismic activity is marked by the strike-slip kinematics. Described structure is a border of Inner and Outer Carpathians. Method of observation: surface observation, geological mapping, geophysics. Strike: W–E in the study area. (Country Report fault code: F-1)
Strefa szwu tektonicznego, ciągnąca się od Alp wzdłuż całego łańcucha karpackiego, tworząca granicę między mikropłytą ALCAPA na południu i płytą euroazjatycką na północy. Powstała w neogenie podczas akrecji mikropłyty ALCAPA. Doskonale rozpoznana w trakcie kartowania geologicznego i rejestrowana metodami geofizycznymi. Współczesna aktywność sejsmiczna ma kinematykę przesuwczą. Opisana struktura wyznacza granicę Karpat Wewnętrznych i Zewnętrznych. Metody obserwacji: odsłoniecia, kartowanie geologiczne, geofizyka. Bieg: W–E w badanym obszarze. (Kod uskoku w Raporcie krajowym projektu HIKE: F-1)
Pieniński Pas Skałkowy
East European Craton (tectonic megadomain)
Megadomena tektoniczna zajmująca północno-wschodnią część Polski (i północno-wschodnią Europę), czyli polski fragment kratonu wschodnioeuropejskiego, składający się z podłoża krystalicznego (skał paleo- i mezoproterozoicznych), pokrywy osadowej skał neoproterozoicznych, paleozoicznych i mezozoicznych oraz uskoków przecinających tę domenę.
Kraton wschodnioeuropejski
East European Craton
Tectonic megadomain occupying the NE half of Poland (and the NE half of Europe), i.e. the Polish fragment of the East European Craton, consisting of Paleo- and Mezoproterozoic crystalline basement and Neoproterozoic, Palaeozoic and Mezozoic cover and faults cross-cutting this domain.
Mazowsze tectonic domain
Tectonic boundary defined on the basis of regional magnetic and gravimetric anomalies pattern.
Granica tektoniczna wyznaczona na podstawie regionalnych anomalii magnetycznych i grawimetrycznych.
Domena mazowiecka
Mazowsze fault zone
Y-shaped magnetic and gravimetric anomalies north of the TTZ, central Poland, close to Mława syenite intrusion. Method of observation: magnetic anomaly map, seismic profiles. Strike: NW–SE. (Country Report fault code: A-8)
Anomalie magnetyczne i grawimetryczne w kształcie litery Y na północ od TTZ, środkowa Polska, w pobliżu intruzji sjenitowej Mławy. Metoda obserwacji: mapa anomalii magnetycznej, profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-8)
Strefa uskokowa Mazowsza
Pomorze–Blekinge Belt
Nasunięcie / granica tektoniczna określona na podstawie regionalnych anomalii magnetycznych i grawimetrycznych.
Pasmo Pomorze–Blekinge
Pomorze–Blekinge border
Nappe / tectonic boundary defined on the basis of regional magnetic and gravimetric anomalies pattern.
Żarnowiec fault zone
System uskoków definiowany na podstawie segmentacji bloków podłoża i przekroju sejsmicznego.
Strefa uskokowa Żarnowca
Fault system defined on the basis segmentation of basement blocks and seismic cross section.
Sambia fault zone
Basement fault zone reactivated during Early Palaeozoic and recently seismically active (2004 earthquakes with max. mag. M5.3) Method of observation: seismic profiles, borehole data, seismic events. (Country Report fault code: A-7)
Strefa uskokowa podłoża reaktywowana we wczesnym paleozoiku, ostatnio aktywna sejsmicznie (trzęsienia ziemi w 2004 r. maksymalna Mag. M5.3) Metoda obserwacji: profile sejsmiczne, dane z otworów wiertniczych, zdarzenia sejsmiczne. (Kod uskoku w Raporcie krajowym projektu HIKE: A-7)
Strefa uskokowa Sambii
Kuźnica fault zone
This fault is deeply rooted in the Proterozoic basement and reactivated after Devonian. Method of observation: seismic profiles, magneto telluric. Strike: N–S. (Country Report fault code: A-6)
Uskok głęboko zakorzeniony w podłożu proterozoicznym, reaktywowany po dewonie. Metody obserwacji: profile sejsmiczne, magnetotelluryka. Bieg: N–S. (Kod uskoku w Raporcie krajowym projektu HIKE: A-6)
Strefa uskokowa Kuźnicy
Uskok w podłożu (?) reaktywowany po dewonie, prawdopodobnie w okresie waryscyjskim. W podkenozoicznym pietrze strukturalnym obserwuje się znaczącą zmienność po przeciwnych stronach tej strefiy uskokowej. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: N–S. (Kod uskoku w Raporcie krajowym projektu HIKE: A-5)
Strefa uskokowa Karwii
Basement(?) fault reactivated after Devonian, probably during Variscan stage. Significant changes in sub-Cenozoic structural level is observed across this fault zone. Method of observation: seismic profiles, borehole data. Strike: N–S. (Country Report fault code: A-5)
Karwia fault zone
Łeba fault zone
Fault zone parallels the TTZ, deeply rooted in the Proterozoic basement, and reactivated in the Palaeozoic and end Creataceous times. Method of observation: seismic profiles, magneto telluric. Strike: NW-SE. (Country Report fault code: A-4)
Strefa uskokowa równoległa do TTZ, głęboko zakorzeniona w podłożu proterozoicznym, reaktywowana w paleozoiku i późnej kredzie. Metody obserwacji: profile sejsmiczne, magnetotelluryka. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-4)
Strefa uskokowa Łeby
Łeba fault zone 2
Łeba fault zone 1
Smołdzino fault zone
Fault zone parallels the TTZ, deeply rooted in the Proterozoic basement and reactivated in Palaeozoic. Method of observation: seismic profiles, magneto telluric. Strike: N–S. (Country Report fault code: A-3)
Strefa uskokowa równoległa do TTZ, głęboko zakorzeniona w podłożu proterozoicznym, reaktywowana w paleozoiku. Metody obserwacji: profile sejsmiczne, magnetotelluryka. Bieg: N–S. (Kod uskoku w Raporcie krajowym projektu HIKE: A-3)
Strefa uskokowa Smołdzina
Ustka fault zone
Fault zone parallels the TTZ, deeply rooted in the Proterozoic basement and reactivated in Palaeozoic and, slightly, later. Method of observation: seismic profiles, magneto telluric. Strike: NW–SE. (Country Report fault code: A-2)
Strefa uskokowa równoległa do TTZ, głęboko zakorzeniona w podłożu proterozoicznym, reaktywowana w paleozoiku, a także później. Metody obserwacji: profile sejsmiczne, magnetotelluryka. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-2)
Strefa uskokowa Ustki
Darłowo fault zone
Fault zone parallels the TTZ, deeply rooted in the Proterozoic basement and reactivated in the Palaeozoic and end Creataceous times. Method of observation: seismic profiles, magneto telluric. Strike: NW–SE. (Country Report fault code: A-1)
Strefa uskokowa równoległa do TTZ, głęboko zakorzeniona w podłożu proterozoicznym, reaktywowana w paleozoiku i późnej kredzie. Metody obserwacji: profile sejsmiczne, magnetotelluryka. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-1)
Strefa uskokowa Darłowa
Mazury Complex
Tectono-metamorphic unit of the East European Craton forming a 200 km long and 40 km wide zone of of granitoids and anorthosite /norite massifs and associated faults, that crosscuts the granulite and amphibolite facies domains in NE Poland.
Jednostka tektoniczno-metamorficzna kratonu wschodnioeuropejskiego tworząca strefę granitoidów i masywy anortozytowe / norytowe o długości 200 km i szerokości 40 km przecinającą domeny facji granulitowych I amfibolitowych w północno-wschodniej Polsce.
Kompleks mazurski
Mazury fault zone
A regional E–W trending lineament in northern Poland and southern Lithuania detected by magnetic and gravimetric mapping. Method of observation: magnetic anomaly map, seismic profiles. Strike: WNW–ESE. (Country Report fault code: A-10)
Reginalny lineament E–W w północnej Polsce i południowej Litwie wykryty za pomocą badań magnetycznych i grawimetrycznych. Metoda obserwacji: mapa anomalii magnetycznej, profile sejsmiczne. Bieg: WNW – ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-10)
Mazurska strefa uskokowa
Mazury fault 1
Mazury fault 3
Mazury fault 2
Płock Trough
The Płock trough is located over the slope of the pre-Vendian East European Platform and the Teisseyre-Tornquist tectonic zone. It developed in its present form at the turn of the Cretaceous and Tertiary but its basement, especially the segmentation of underlying platform sediments, reveal older roots.
Niecka Płocka położona na skłonie przedwendyjskiej platformy wschodnioeuropejskiej i strefy tektonicznej Teisseyre-Tornquista. Obecny kształt niecki powstał na przełomie kredy i trzeciorzędu. Podłoże niecki, zwłaszcza tektoniczna segmentacja niżej leżących osadów pokrywy platformowej, ujawnia starsze korzenie.
Niecka płocka
Żuromin–Płońsk fault zone
Probably basement fault reactivated in Late Cretaceous in a form of narrow anticlines bounded with reverse faults accommodated in the Zechstein salt. Method of observation: seismic profiles, borehole data. Strike: NW–SE to WNW–ESE. (Country Report fault code: A-18)
Prawdopodobny uskok podłoża reaktywowany w późnej kredzie w postaci wąskich antyklin ograniczonych uskokami odwróconymi, powiązanymi z solami cechsztyńskimi. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: NW–SE do WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-18)
Strefa uskokowa Żuromin–Płońsk
Lublin Basin
Devonian–Carboniferous fault-controlled basin developed within the Variscan foreland over the SW limit of the east European Craton [the Teisseyre-Tornquist Zone (TTZ)] and then inverted at the end of the Variscan orogeny.
Dewońsko–karboński basen lubelski, który rozwinął się na przedpolu waryscyjskim na granicy z kratonem wschodnioeuropejskim [strefa Teisseyre-Tornquista (TTZ)], a następnie uległ inwersji pod koniec orogenezy waryscyjskiej.
Basen lubelski
Grójec fault
Deeply-rooted basement fault zone reactivated during Late Paleozoic subsidence and inversion of the Lublin Basin. The kinematics is unknown. Representation in the magnetic and gravimetric anomaly fields points to its trans-crustal range. Method of observation: seismic profiles, potential fields data. Strike: NE–SW. (Country Report fault code: A-17)
Głęboko zakorzeniona strefa uskoków podłoża reaktywowana podczas późno-paleozoicznej subsydencji a następnie inwersji niecki lubelskiej. Kinematyka jest nieznana. Obraz anomalii magnetycznych i grawimetrycznych wskazuje na strefę o zasięgu skorupowym. Metoda obserwacji: profile sejsmiczne, dane dotyczące pól potencjalnych. Bieg: NE–SW. (Kod uskoku w Raporcie krajowym projektu HIKE: A-17)
Uskok Grójca
Grójec fault 1
Grójec fault 2
Niedrzwica–Bełżce fault system
Minor reverse faults developed on both sides of the thin-skinned anticlinal structure due to the basin inversion in Late Carboniferous. Basement faults control on the thrust location is possible. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: A-16)
Niewielkie uskoki odwrócone powstałe po obu stronach naskórkowej struktury antyklinalnej w wyniku inwersji basenu w późnym karbonie. Możliwa jest korelacja z uskokami podłoża. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-16)
System uskokowy Niedrzwica–Bełżce
Ciecierzyn fault system
Minor reverse faults developed on both sides of the thin-skinned anticlinal structure due to the basin inversion in Late Carboniferous. Basement faults control on the thrust location is possible. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: A-15)
Niewielkie uskoki odwrócone powstałe po obu stronach naskórkowej struktury antyklinalnej w wyniku inwersji basenu w późnym karbonie. Możliwa jest korelacja z uskokami podłoża. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-15)
System uskokowy Ciecierzyn
Izbica–Zamość fault zone
Thrust faults with the NE vergence with secondary back-thrusts. Thin-skinned structures developed during the Late Carboniferous basin inversion. Basement faults control on the thrust location is possible. Method of observation: seismic profiles, borehole data. Strike: NW–SE to WNW–ESE. (Country Report fault code: A-14)
Nasunięcia o wergencji NE oraz nasunięcia wsteczne niższego rzędu. Powstały na etapie inwersji basenu w późnym karbonie jako struktury tektoniki naskórkowej. Struktura prawdopodobnie rozwinięta ponad uskokami podłoża. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: NW–SE do WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-14)
Strefa uskokowa Izbica–Zamość
Janów fault zone
Wilczopole–Marynin–Radawiec fault zone
Main thrust faults with NE vergence with secondary back-thrusts. Thin-skinned structures developed during the Late Carboniferous basin inversion. Basement faults control on the thrust location is possible. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: A-13)
Nasunięcie główne o wergencji NE oraz nasunięcia wsteczne niższego rzędu. Powstały na etapie inwersji basenu w późnym karbonie jako struktury tektoniki naskórkowej. Struktura prawdopodobnie rozwinięta ponad uskokami podłoża. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-13)
Strefa uskokowa Wilczopole-Marynin-Radawiec
Ursynów–Kazimierz fault set
Set of parallel faults composed of the basement-involved faults active during basin subsidence stage and thin-skinned thrusts of the Carboniferous age related to basin inversion. Minor back thrusts are present. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: A-12)
Zespół równoległych uskoków zakorzenionych w podłożu, aktywny w tracie subsydencji basenu, a następnie na etapie inwersji basenu w karbonie jako nasunięcia tektoniki naskórkowej. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-12)
Uskoki Ursynów-Kazimierz
Kazimierz–Ursynów fault
Kock fault zone
Fault zone composed of the basement-involved Early Paleozoic fault downthrowing the NE wall, inverted during the Late Fammenian and then cut and displaced to the NE by a thin-skinned thrust, decoupled in the Silurian shales, during the Late Westphalian phase of the Variscan orogeny. The secondary back-thrusts are also present. Method of observation: seismic profiles, borehole data. Strike: NW–SE to WNW–ESE. (Country Report fault code: A-11)
Strefa uskokowa podłoża rozwinięta we wczesnym paleozoiku, o zrzutowym skrzydle NE, odwrócona w późnym famenie, a następnie przecięta i przesunięta ku NE nasunięciem naskórkowym, odkłutym w łupkach syluru podczas późnej westfalskiej fazy orogenezy waryscyjskiej. Występują tu również nasunięcia wsteczne niższego rzędu. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: NW–SE do WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-11)
Strefa uskokowa Kocka
Kock fault
Narol fault
Major fault system, observed on the basis of deep reflection seismic profile Polcrust 01.
Regionalny system uskokowy obserwowany w głębokim profilu refleksyjnym Polcrust 01.
Uskok Narola
Biłgoraj Narol zone
Hanna fault
Tectonic boundary defined on the basis of regional magnetic and gravimetric anomalies pattern and differences of the crystalline basement depth.
Granica tektoniczna zdefiniowana na podstawie ukladu regionalnych anomalii magnetycznych i grawimetrycznych i różnicy głębokości podłoża.
Uskok Hanny
Podlasie–Bielarus Granulite Belt
Crustal domain trending NE–SW between western Bielarus and TTZ, displaying arcuate, high-positive magnetic anomalies in its eastern part. In Poland it includes a greater part of the Podlasie fold zone and the metamorphic Kampinos complex. A belt of positive magnetic anomalies, interpreted as Białystok fault, defines its NW border.
Domena skorupowa z łukowatymi silnie dodatnimi anomaliami magnetycznymi we wschodniej części, o przebiegu NE–SW od zachodniej Białorusi do TTZ. Na obszarze Polski obejmuje większą część podlaskiej strefy fałdowej i metamorficznego kompleksu kampinoskiego. NW granicę jednostki wyznacza pasmo wyżów magnetycznych interpretowane jako uskok Białegostoku.
Podlasko–Białoruski pas granulitowy
Białystok fault zone
The border of Palaeoproterozoic structure known as the Belarus Podlasie Granulite belt. SW–NE trending zone of the prominent regional magnetic anomaly interpreted as major shear zones, related to the 1.82 Ga – 1.80 Ga Fennoscandia-Sarmatia collision. Method of observation: magnetic anomaly map, seismic profiles. Strike: WNW–ESE. (Country Report fault code: A-9)
Granica struktury paleeoproterozoicznej zwanej pasem granulitowym Białoruś–Podlasie. Strefa z trendem SW–NE widoczna w regionalnej anomalii magnetycznej, zinterpretowana została jako główne strefy ścinania, związana z kolizją 1,82 Ga - 1,80 Ga Fennoskandia-Sarmcja. Metoda obserwacji: mapa anomalii magnetycznej, profile sejsmiczne. Bieg: WNW – ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: A-9)
Strefa uskokowa Białegostoku
Białystok fault 5
Białystok fault 4
Białystok fault 3
Białystok fault 2
Białystok fault 1
Upper Sileasian fault zones
Faults cross-cutting the Upper Silesian Block (see below).
Uskoki przecinające blok górnośląski.
Strefy uskokowe bloku górnośląskiego
Upper Silesian Block
Upper Silesian block is the Northern part of a complex Brunovistulicum terrane. Within Polish borders, its western limit is the Moldanubian thrust belt, its northern and eastern border is the Kraków–Lubliniec fault zone and its southern limit is the peri-Pieniny fault zone.
Blok górnośląski stanowi północną część złożonego terranu Brunovistulicum. W granicach Polski zachodnią granicę tej jednostki wyznacza strefa nasunięć moldanubskich, północą i wschodnią strefa uskokowa Kraków–Lubliniec, południową perypienińska strefa uskokowa.
Blok górnośląski
Kraków–Lubliniec fault zone
Shear zone, active from the Neoproterozoic to the Mesozoic, with multiple strike-slip deformations, with the dominant phases at the turn of the Silurian/Devonian and in the Late Variscan time. Described structure is an edge of Upper Silesian and Małoposka Block. Additionally it’s a part of Hamburg–Kraków Tectonic Zone. Method of observation: gravimetry, borehole data, geological mapping. Strike: NW–SE. (Country Report fault code: D-1)
Strefa ścinania, aktywna od neoproterozoiku do mezozoiku, z licznymi deformacjami przesuwczymi, z dominującymi fazami na przełomie syluru / dewonu i późnych ruchów waryscyjskich. Opisywana struktura stanowi skraj bloku górnośląskiego i małoposkiego. Dodatkowo jest częścią strefy tektonicznej Hamburg–Kraków. Metody obserwacji: grawimetria, dane z otworów wiertniczych, kartografia geologiczna. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: D-1)
Strefa uskokowa Kraków–Lubliniec
Żywiec – Nowy Sącz fault set
Subparallel normal faults of the Late Variscan origin, reactivated until Cenozoic, systematically downthrowing the southern walls by 400–600 m. They form the southern edge of the Bielsko-Biała elevation. Described structure is a border of Upper Silesian Block and Bielsko-Biała dome. Method of observation: geological mapping. Strike: W–E. (Country Report fault code: D-8)
Późnowaryscyjskie równoległe uskoki normalne, aktywne aż do kenozoiku, systematycznie zrzucające południowe skrzydła o o 400–600 m. Tworzą południowy kraniec elewacji Bielska-Białej. Opisywana struktura stanowi granicę bloku górnośląskiego i kopuły Bielska-Białej. Metoda obserwacji: kartowanie geologiczne. Bieg: W–E. (Kod uskoku w Raporcie krajowym projektu HIKE: D-8)
Zespół uskoków Żywiec – Nowy Sącz
Ruptawa and Jawiszowice fault set
Subparallel normal faults of the Late Variscan origin, reactivated until Cenozoic, systematically downthrowing theis southern walls by 400–700 m. They form the northern boundary of the Neogene Carpathian Foredeep Basin. Described structure is a border of Upper Silesian Block and the Carpathian Foredeep. Method of observation: borehole data, mining and geological mapping. Strike: W–E. (Country Report fault code: D-7)
Późnowaryscyjskie równoległe uskoki normalne, aktywne aż do kenozoiku, systematycznie zrzucające południowe skrzydła o 400–700 m. Tworzą północną granicę neogeńskiego zapadliska przedkarpackiego. Opisywana struktura stanowi granicę bloku górnośląskiego i zapadliska przedkarpackiego. Metody obserwacji: dane otworowe, mapy górnicze i geologiczne. Bieg: W–E. (Kod uskoku w Raporcie krajowym projektu HIKE: D-7)
Zespół uskoków Ruptawy i Jawiszowic
Moravian–Silesian Fold and Thrust Belt
Moravian–Silesian fold and thrust belt formed due to the Late Variscan collision of the Brunovistulicum terrane with the Czechia Massif. It is made of deformed Proterozoic and and Devonian cristalline rocks, Carboniferous flysh and Carboniferous coal-bearing rocks, occuring between Moldanubian thrusts in the west and the Orlova–Boguszowice thrust in the east. Structural style is a fold-and-thrust belt with roughly N–S trending folds showing predominantly eastern vergence.
Morawsko-śląskie pasmo fałdowo-nasuwcze, utworzyło się w wyniku późnowaryscyjskiej kolizji Brunovistulicum z masywem czeskim. Obejmuje zdeformowane proterozoiczne i dewońskie skały krystaliczne, karbońskie utwory fliszowe i karbońskie utwory węglonośne położone między strefą nasunięć moldanubskich na zachodzie a nasunięciem orłowsko–boguszowickim na wschodzie. Obszar cechuje się fałdowo-nasunięciowym stylem budowy, struktury fałdowe wykazują subpołudnikowy przebieg oraz przeważnie wschodnią wergencję.
Morawsko–śląski pas fałdowo-nasunięciowy
Orlova–Boguszowice Thrust
A set of thrust faults of the eastern vergence, forming Variscan deformation front, overthrusted on the Upper Silesian foredeep basin. Method of observation: borehole data, mining and geological mapping. Strike: NNE–SSW. (Country Report fault code: D-6)
Zespół nasunięć o wschodniej wergencji tworzących front deformacji waryscyjskich, nasuniętych na (przedgórski) basen górnośląski. Metody obserwacji: dane otworowe, mapy górnicze i geologiczne. Bieg: NNE–SSW. (Kod uskoku w Raporcie krajowym projektu HIKE: D-6)
Nasunięcie Orlowej–Boguszowic
Andrychów–Chyżne fault set
Contact zone between Precambrian terranes, reactivated after the Permian. Method of observation: magnetotellurics, borehole data, geological mapping. Strike: NNW–SSE. (Country Report fault code: D-5)
Strefa kontaktu między terranami prekambryjskimi, reaktywowana po permie. Metoda obserwacji: magnetotelluryka, dane otworowe, kartowanie geologiczne. Bieg: NNW–SSE. (Kod uskoku w Raporcie krajowym projektu HIKE: D-5)
Zespół uskoków Andrychów–Chyżne
Rzeszotary fault set
Tectonic horst with elevated Archaic–Proterozoic basement of the Upper Silesia Block bounded by steep faults showing vertical displacement > 1500 m, active in the Neoproterozoic and Late Variscan times. Method of observation: gravimetry borehole data, geological mapping. Strike: NNW–SSE. (Country Report fault code: D-4)
Zrąb tektoniczny z wyniesionym archaiczno-proterozoicznym podłożem bloku górnośląskiego, ograniczonym stromymi uskokami o przemieszczeniach pionowych > 1500 m, czynny w okresie neoproterozoiku i późnych ruchów waryscyjskich. Metoda obserwacji: dane grawimetryczne z otworów wiertniczych, kartowanie geologiczne. Bieg: NNW–SSE. (Kod uskoku w Raporcie krajowym projektu HIKE: D-4)
Zespół uskoków Rzeszotar
Tworóg–Zawiercie fault set
Fault zone founded in Cadomian time and repeatedly reactivated until the Cenozoic; creates the boundary between the elevated Brudzowice (Siewierza) Block and the Permian Sławków Graben. The final vertical offset is >1000 m. Method of observation: gravimetry, borehole data, geological mapping. Strike: WNW–ESE. (Country Report fault code: D-3)
Strefa uskokowa założona w trakcie orogenezy kadomskiej i wielokrotnie reaktywowana aż do kenozoiku; tworzy granicę pomiędzy wyniesionym blokiem Brudzowic (Siewierza) a permskim rowem Sławkowa. Całkowity pionowy zrzut wynosi> 1000 m. Metody obserwacji: grawimetria, dane z otworów wiertniczych, kartografia geologiczna. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: D-3)
Zespół uskoków Tworóg–Zawiercie
Krzeszowice–Charsznica fault
Strike-slip fault, which accomodated 12 km transversal sinistral offset of the Kraków–Lubliniec Fault Zone at the end of the Variscan orogeny. Described structure is the limit between the Upper Silesia and Małoposka blocks. Method of observation: geological mapping. Strike: NNE–SSW. (Country Report fault code: D-2)
Uskok lewo-przesuwczy, który pod koniec orogenezy waryscyjskiej zaabsorbował 12 kilometrów przesunięcia wzdłuż strefy uskokowej Kraków–Lubliniec. Opisana struktura stanowi granicę między blokiem Górnego Śląska i Małoposki. Metoda obserwacji: kartowanie geologiczne. Bieg: NNE–SSW. (Kod uskoku w Raporcie krajowym projektu HIKE: D-2)
Uskok Krzeszowice–Charsznica
Lower Silesian fault systems and zones
Set of polygenetic and multidirectional fault systems and zones, mostly originating from Variscan orogeny (Carboniferous) or Permian to Mesozoic mainly extensional events, partly inverted by Late Cretaceous–Palaeogene compressional episode and reactivated by Late Cenozoic tectonic activity at the distant foreland of Alps and Carpathians.
Zbiór poligenetycznych i wielokierunkowych systemów i stref uskoków, powstałych głównie podczas orogenezy waryscyjskiej (karbońskiej) lub permo-mezozoicznych epizodów ekstensyjnych. Uskoki te częściowo uległy inwersji w trakcie późnokredowej i paleogeńskiej kompresji a także zostały reaktywowane przez późnokenozoiczną aktywność tektoniczną na dalekim przedpolu Alp i Karpat.
Systemy i strefy uskokowe Dolnego Śląska
Fore-Sudetic homocline faults
Multi-stage faults, often decoupled across Permian salts, cross-cutting shallow NNE- to NE-dipping Permo–Mesozoic succession, defining the SW limb of the Szczecin–Miechów trough (synclinorium), NE of the Middle Odra fault system.
Wielokrotnie odmładzane uskoki, często odspojone w solach permskich, przecinające łagodnie zapadającą na NNE do NE serię permo-mezozoiczną, wyznaczającą SW skrzydło niecki szczecińsko-miechowskiej (synklinorium) na północny-wschód od systemu uskoków Środkowej Odry.
Uskoki monokliny przedsudeckiej
Dolsk fault zone
Blind fault zone buried below thick Permo–Mesozoic succession. Originally a Variscan, Carboniferous dextral strike-slip, possibly reactivated in later times. On deep seismic profiles separates different crust types: 3-layer one typical of Baltica and Palaeozoic Platform to the NE and a low-velocity 2-layer one to the SW – typical of the Variscan belt. Method of observation: industrial seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: E-1)
Strefa uskokowa w podłożu miąższej sukcesji skał permo-mezozoicznych. Pierwotnie karboński, prawoprzesuwczy uskok waryscyjski, prawdopodobnie później reaktywowany. Na głębokich profilach sejsmicznych rozdziela różne typy skorupy: 3-warstwową typową dla Baltiki i platformy paleozoicznej na NE i 2-warstwową o niskich prędkościach na SW – typową dla pasa waryscyjskiego. Metoda obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: E-1)
Strefa uskokowa Dolska
Poznań–Oleśnica fault system
Large-scale complex graben system, following the originally Triassic fault train, of possible Variscan antecedence, evolved through Mesozoic extensional events to, eventually, form a system of branching tectonic grabens with Late Cenozoic lignite deposits. Includes grabens of: (1) Poznań–Oleśnica, (2) Chruścina, (3) Chobienia–Rawicz. Method of observation: potential field and drilling record. Strike: NW–SE to ENE–WSW for branches. (Country Report fault code: E-2)
System rowów, przebiegający zgodnie z ciągiem uskoków triasowych, o możliwym założeniu waryscyjskim, ewoluował w wyniku epizodów ekstensji w mezozoiku, ostatecznie tworząc system rozgałęzionych rowów tektonicznych ze złożami późnokenozoicznego węgla brunatnego. Zawiera rowy: (1) Poznań–Oleśnica, (2) Chruścina, (3) Chobienia–Rawicz. Metoda obserwacji: pola potencjalne i wiercenia. Bieg: od NW–SE do ENE–WSW. (Kod uskoku w Raporcie krajowym projektu HIKE: E-2)
System uskokowy Poznań–Oleśnica
Opole Trough
Fragment of Upper Cretaceous sedimentary cover erosionally separated from that of the Szczecin–Miechów trough, preserved in a tectonic depression resting on top of older Permo–Mesozoic and Carboniferous strata and Varisan crystalline basement.
Fragment górnokredowej pokrywy osadowej, oddzielonej erozyjnie od niecki szczecińsko-miechowskiej, zachowany w obniżeniu tektonicznym, na warstwach permo–mezozoicznych i karbońskich oraz krystalicznym podłożu waryscyjskim.
Niecka opolska
Paczków and Kędzierzyn graben system
A chain of the Late Cenozoic grabens, developed mostly in the Miocene, probably due to extension in the foreland plate of the folded Carpathians. Method of observation: borehole data, seismic profiles. Strike: W–E. (Country Report fault code: E-9)
Łańcuch późno kenozoicznych rowów, rozwinął się głównie w miocenie, prawdopodobnie w wyniku ekstensji na przedpolu Karpat. Metody obserwacji: dane z otworów wiertniczych, profile sejsmiczne. Bieg: W–E. (Kod uskoku w Raporcie krajowym projektu HIKE: E-9)
System rowów Paczkowa i Kędzierzyna
Sudetic block
Late Miocene-uplifted SW part of the Lower Silesia block, limited by the Sudetic Boundary fault in the NW and extending to Czechia to the SW.
Południowo-zachodnia część bloku dolnośląskiego wyniesiona w późnym miocenie, ograniczona uskokiem brzeżnym sudeckim na NW i sięgająca na SW do Czech.
Blok sudecki
Upper Nysa Kłodzka River graben system
A system developed from the end of Cretaceous through Late Cenozoic, initially some of its faults originated as reverse, subsequently turned into normal faults downthrowing the Upper Nysa Graben and adjacent smaller depressions. These faults are part of a larger system that continues into Czechia as the Pořiči–Hronov Fault Zone. Described structure is a border of Sudetic Nysa Graben and Kłodzko–Orlica Dome. Includes faults of: Chocieszów, Pstrążna–Gorzanów, Zieleniec, Jagodna–Młoty. Method of observation: topographic expression, geological mapping. Strike: N–S to NW–SE. (Country Report fault code: E-8)
System rozwijał się od końca kredy do późnego kenozoiku, początkowo niektóre jego uskoki były uskokami odwróconymi, a następnie przekształciły się w uskoki normalne zrzucające rów Górnej Nysy i przyległe mniejsze obniżenia. Uskoki te są częścią większego systemu, który ciągnie się do Czech jako strefa uskoku Pořiči–Hronov. Opisywany system stanowi granicę sudeckiego rowu Nysy i wyniesienia kopuły Kłodzko–Orlickiej. W skład systemu wchodzą uskoki: Chocieszów, Pstrążna–Gorzanów, Zieleniec, Jagodna–Młoty. Metody obserwacji: analiza topografii, kartowanie geologiczne. Bieg: z N–S do NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: E-8)
System rowów górnej Nysy Kłodzkiej
North Karkonosze fault system
A system of Cenozoic normal faults responsible for downthrowing the Jelenia Góra Basin with respect to the Karkonosze, Rudawy Janowickie, Izera and Kaczawa Mts. Described structure is a border of Sudetic Block and Izera–Karkonosze Massif. Method of observation: topographic expression, surface observations. Strike: WNW—ESE and NE-SW. (Country Report fault code: E-7)
System kenozoicznych uskoków normalnych odpowiedzialnych za obniżenie Kotliny Jeleniogórskiej w stosunku do Karkonoszy, Rudaw Janowickich, Izery i Kaczaw. System wyznacza granicę Bloku Sudeckiego i Masywu Izersko–Karkonoskiego. Metody obserwacji: analiza topografii, obserwacje powierzchniowe. Bieg: WNW–ESE i NE–SW. (Kod uskoku w Raporcie krajowym projektu HIKE: E-7)
Północno karkonoski system uskokowy
Turoszów–Żytawa fault system
Faults delineating the Siekierczyn and Zittau Troughs (grabens) filled with lignite formation at the NE termination of the extensive Ohře (Eger) Graben of NW Czechia, related to Late Cenozoic abundant basaltoid volcanism. Described structure is a border of Sudetic Block, Turoszów–Żytawa Trough (synclinorium) and Izera–Karkonosze Massif. Method of observation: surface observations, topographic expression, mining data. Strike: NNE–SSW and WNW–ESE. (Country Report fault code: E-6)
Uskoki wyznaczające niecki siekierczyńską j i żytawską. Niecki wypełnione węglem brunatnym, położone w NE części rozległego rowu Ohře (Eger) północno-zachodnich Czech, związane z wulkanizmem bazaltoidowym późnego kenozoiku. Opisywane struktury stanowią granicę bloku sudeckiego, niecki Turoszów–Żytawa i Masywu Izersko–Karkonoskiego. Metody obserwacji: obserwacje powierzchniowe, analiza topografii, dane górnicze. Bieg: NNE–SSW i WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: E-6)
System uskokowy Turoszów–Żytawa
Intra-Sudetic fault zone
A major, NW–SE trending ductile shear zone/semi-brittle to brittle fault zone, in most parts exposed on the surface. The main activity occurred in Carboniferous times, with estimated dextral displacement of at least 50 km, but possibly reaching as much as ~300 km. This was followed by Late Carboniferous reversal with a sinistral displacement of ~25 km and Permian to Neogene dip-slip. Method of observation: field observations, potential field record. Strike: NNW–SSE. (Country Report fault code: E-5)
Duża strefa ścinania o kierunku NW–SE przechodząca w strefę uskoków półkruchych do kruchych, w znacznej części widoczna w odsłonięciach. Główna aktywność miała miejsce w karbonie, szacowane przemieszczenie (prawoskrętne) to co najmniej 50 km, ale może sięgać nawet ~ 300 km. W późnym karbonie nastąpiło odwrócenie kierunku ruchu (przesunięcie lewoskrętne), szacowana wielkość tego przemieszczenia to ~ 25 km, następnie deformacje zrzutowe od permu do neogenu. Metoda obserwacji: obserwacje terenowe, pomiary pól potencjalnych. Bieg: NNW–SSE. (Kod uskoku w Raporcie krajowym projektu HIKE: E-5)
Strefa uskoku śródsudeckiego
Sudetic Boundary (Marginal) fault system
Fault zone prominently expressed in the Sudetic topography. Originally, a probable large-scale Riedel shear accompanying the Carboniferous displacement on the Intra-Sudetic Fault Zone. Subsequently reactivated with a dip-slip kinematics: (1) at the Cretaceous/Palaeogene turn, uplifting the Fore-Sudetic block with respect to the Sudetic one; (2) in the Late Miocene, reversing the position of the Sudetic vs Fore-Sudetic blocks. Additionally, described structure is a part of Elbe Fault Zone. Method of observation: field observations, potential field record, magnetotelluric data. Strike: NW–SE to NNW–SSE. (Country Report fault code: E-4)
Strefa uskokowa wyraźnie zaznaczona w topografii Sudetów. Pierwotnie prawdopodobnie wielkoskalowe ścięcie Riedla, towarzyszące karbońskiemu przemieszczeniu na uskoku śródsudeckim. Następnie reaktywowana w reżimie zrzutowym: (1) na przełomie kredy / paleogenu, wynosząc blok przedsudecki względem sudeckiego; (2) w późnym miocenie, odwracając położenie bloku sudeckiego względem przedsudeckiego. Opisywana struktura jest częścią strefy uskokowej Łaby. Metoda obserwacji: obserwacje terenowe, pomiary pól potencjalnych, dane magnetotelluryczne. Bieg: NW–SE do NNW–SSE. (Kod uskoku w Raporcie krajowym projektu HIKE: E-4)
System uskokowy uskoku brzeżnego sudeckiego
Middle Odra fault system
Originally a Variscan, Carboniferous dextral strike-slip major fault zone injected with Carboniferous granitoids, recurrently reactivated in the Permo–Mesozoic cover, mostly in dip-slip regime in times between Permian and Neogene. At present, does not show clear topographic effects of its youngest possible activity, except for its trace being followed by the Odra river. Described structure is a border of Sudetic Block and Fore-Sudetic Block. It’s also presumably a part of Hamburg–Kraków Fault Zone. Method of observation: borehole data, potential field, sparse seismic profiles, copper mines data. Strike: NW–SE to WNW–ESE. (Country Report fault code: E-3)
Pierwotnie waryscyjska, karbońska, prawoskrętna strefa uskoku przesuwczego, z karbońskimi intruzjami granitoidów, z widoczną w pokrywie permo-mezozoicznej reaktywacją, głównie w reżimie zrzutowym, w okresie między permem a neogenem. Obecnie w topografii przejawia się jedynie w przebiegu doliny Odry. Opisana struktura wyznacza granicę bloku sudeckiego i przedsudeckiego. Przypuszczalnie jest też częścią strefy uskokowej Hamburg–Kraków. Metody obserwacji: dane z otworów wiertniczych, pola potencjalne, skąpe profile sejsmiczne, dane z kopalni miedzi. Bieg: NW–SE do WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: E-3)
System uskokowy środkowej Odry
Northern segment of the Trans-European suture zone
Trans-European suture zone (TESZ) is a litospheric-scale tectonic suture between the East European Craton and the Palaeozoic West European Platform.
TESZ to szew tektoniczny stanowiący granicę między kratonem wschodnioeuropejskim a platformą paleozoiczną Europy Zachodniej.
Północna część strefy szwu transeuropejskiego
Łódź Trough is a middle part of the Szczecin–Miechów synclinorium, bordering the Mid-Polish Swell/anticlinorium from the SW.
Niecka łódzka jest częścią synklinorium szczecińsko-miechowskiego, przylegającego od południowej strony do antyklinorium środkowopolskiego.
Niecka łódzka
Łódź Trough
Poznań–Kalisz–Wieruszów fault zone
Sigmoidal and branched basement fault system partially reactivated in the T3–J1. Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-19)
Sigmoidalny i rozgałęziony system uskoków podłoża, częściowo reaktywowany w T3–J1. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-19)
Strefa uskokowa Poznań–Kalisz–Wieruszów
Wieluń–Szczerców fault zone
Mezozoiczna strefa uskokokowa, częściowo reaktywowana jako rów mioceński. Strefa ta stanowi granicę niecki łódzkiej i monokliny przedsudeckiej. Metoda obserwacji: profile sejsmiczne. Bieg: W–E. (Kod uskoku w Raporcie krajowym projektu HIKE: B-20)
Strefa uskokowa Wieluń–Szczerców
Mesozoic fault zone partially reactivated as the Miocene graben. Described structure is a border of Łódź Trough (synclinorium) and Fore-Sudetic Monocline. Method of observation: seismic profiles. Strike: W–E. (Country Report fault code: B-20)
Opatówek–Szczerców fault zone
Basement fault zone partially reactivated in the Mesozoic. Described structure is a border of Łódź Trough (synclinorium) and Fore-Sudetic Monocline. Strike: NW–SE. (Country Report fault code: B-18)
Strefa uskokowa podłoża częściowo reaktywowana w mezozoiku. Struktura ta wyznacza granicę niecki łódzkiej i monokliny przedsudeckiej. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-18)
Strefa uskokowa Opatówek–Szczerców
Konin–Bełchatów fault zone
Rooted in the basement, sigmoidal fault zone, partially reactivated in the Mesozoic. Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-17)
Sigmoidalna strefa uskokowa mająca swoje korzenie w podłożu, częściowo reaktywowana w mezozoiku. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-17)
Strefa uskokowa Konin–Bełchatów
Damasławek–Mogilno fault zone
Probably basement fault zone documented in the Mesozoic cover with two salt diapirs activated in the Cenozoic. Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-16)
Prawdopodobnie strefa uskoku podłoża udokumentowana w pokrywie mezozoicznej z dwoma wysadami solnymi aktywnymi w kenozoiku. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-16)
Strefa uskokowa Damasławek–Mogilno
Sompolno–Kcynia–Szubin fault zone
Branched basement fault system reactivated in the Mesozoic with an array of salt diapirs created in the T3–J1. Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-15)
Rozgałęziony system uskoków podłoża reaktywowany w mezozoiku z szeregiem wysadów solnych powstałych na przełomie T3 – J1. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-15)
Strefa uskokowa Sompolno–Kcynia–Szubin
Teisseyre-Tornquist fault zone
A zone of deep, crustal-scale faults delineating the eastern border of the TESZ: a great tectonic boundary defined in regional scale confirmed by deep seismic experiments, regional magnetic and grawimetric mapping.
Strefa głębokich rozłamów stanowiąca wschodnią granicę TESZ, zdefiniowana na podstawie głębokich profilowań sejsmicznych oraz regionalnych map anomalii magnetycznych i grawimetrycznych.
Strefa uskokowa Teisseyre-Tornquista
Teisseyre-Tornquist zone
T-T fault zone 1
Toruń–Radom fault zone
Basement fault zone being the margin of the East European Craton, reactivated in T3–J1 and Late Cretaceous. Method of observation: seismic profiles. (Country Report fault code: B-12)
Strefa uskoku podłoża stanowiąca krawędź kratonu wschodnioeuropejskiego, reaktywowanego w T3–J1 i późnej kredzie. Metoda obserwacji: profile sejsmiczne. (Kod uskoku w Raporcie krajowym projektu HIKE: B-12)
Strefa uskokowa Toruń–Radom
Koszalin–Toruń fault zone
Northernmost segment of the TTZ being the edge of the EEC. Created in Early Paleozoic and reactivated in Cr2 and later(?). Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B- 2)
Najbardziej na N wysunięty segment TTZ będący krawędzią kratonu wschonioeuropejskiego. Utworzony we wczesnym paleozoiku i reaktywowany w górnej kredzie lub później (?). Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B- 2)
Strefa uskokowa Koszalin–Toruń
Miastko–Świecie fault zone
Faulted part of the EEC margin, with the heavily deformed Lower Paleozoic complex, regarded as the front of the Caledonides. Method of observation: seismic profiles, gravimetry. Strike: NW–SE. (Country Report fault code: B-1)
Zuskokowane obrzeże kratonu wschodnioeuropejskiego, z silnie zdeformowanym kompleksem dolnego paleozoiku, uważane za przedpole kaledonidów. Metoda obserwacji: profile sejsmiczne, grawimetria. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-1)
Strefa uskokowa Miastko–Świecie
T-T fault zone 4
T-T fault zone 3
T-T fault zone 2
Pomeranian Swell
Uplifted and elongated tectonic domain (anticlinorium) about 14000 sq. km in area, forming the NW segment of the Mid-Polish Swell/anticlinorium. Its NW part is characterized by multidirectional faults, occurrence of Late Triassic – Early Jurassic synsedimentary grabens and half-grabens incorporated into the overall anticlinorium architecture, the lack of regional salt tectonics, and reduced sequences of the Zechstein and Mesozoic strata. The SE part is marked by well developed non-piercement salt domes of WNW–ESE to NW–SE trends, separated by the extensive zones out of which the Zechstein salts have been completely or almost completely squeezed. The intensity of salt tectonics increases towards SE, where isolated salt pillows merge into elongated salt swells in which the thickness of tectonically accumulated salts exceeds 2000 m.
Wypiętrzona i wydłużona jednostka tektoniczna o powierzchni ok. 14 000 km2, tworząca północno-zachodni odcinek wyniesienia środkowopolskiego. Jej północno-zachodnia część charakteryzuje się wielokierunkowymi uskokami, występowaniem rowów i półrowów synsedymentacyjnych w późnym triasie i wczesnej jurze, brakiem regionalnej tektoniki solnej oraz zredukowanymi sekwencjami warstw cechsztyńskich i mezozoicznych. Część południowo-wschodnia charakteryzuje się dobrze rozwiniętymi nie-przebijającymi wysadami solnymi o kierunkach od WNW–ESE do NW–SE, oddzielonymi rozległymi strefami, z których całkowicie lub prawie całkowicie wyciśnięte zostały sole cechsztyńskie. Intensywność tektoniki solnej rośnie w kierunku południowo-wschodnim, gdzie izolowane poduszki solne łączą się w wydłużone wały solne, w których miąższość soli spiętrzonych tektonicznie przekracza 2000 m.
Wyniesienie Pomorza
Wysoka Kamieńska fault
T3–J1 graben reactivated in Cr2 related to the slip accommodation of the Kamień–Adler basement strike-slip fault zone. Method of observation: seismic profiles. Strike: WNW–ESE. (Country Report fault code: B-5)
Rów T3 – J1 reaktywowany w Cr2 związany z lokalizacją przesuwczej strefy uskokowej podłoża Kamień–Adler. Metoda obserwacji: profile sejsmiczne. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-5)
Uskok Wysoka Kamieńska
Trzebiatów fault zone
Uskoki ograniczające zachowane fragmenty kompleksu kredowego pośrodku wału środkowopolskiego (wał pomorski). Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-4)
Strefa uskokowa Trzebiatowa
Bounding remnants of the Cretaceous complex in the middle of the Mid-Polish Swell/anticlinorium (Pomeranian Swell segment). Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-4)
Kołobrzeg fault zone
Basement fault zone reactivated in the Mesozoic, linking two larger fault zones. Method of observation: seismic profiles. Strike: N–S. (Country Report fault code: B-3)
Strefa uskokowa podłoża, reaktywowana w mezozoiku, łącząca dwie większe strefy uskokowe. Metoda obserwacji: profile sejsmiczne. Bieg: N–S. (Kod uskoku w Raporcie krajowym projektu HIKE: B-3)
Strefa uskokowa Kołobrzegu
Nowogard–Adler fault zone
Uskok podłoża ograniczający od strony południowo-zachodniej wał środkowopolski (wał pomorski) . W T3–J1 uskok ten kontrolował rozwój rowów typu en echelon. Niewielka reaktywacja w późnej kredzie. Opisywany obiekt stanowi granicę wału pomorskiego i niecki szczecińskiej. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-8)
Strefa uskokowa Nowogard–Adler
Basement fault bounding Mid-Polish Swell/anticlinorium (Pomeranian Swell segment) from the SW. In the T3–J1 this fault controlled development of en echelon horse-tail grabens. Minor reactivation in the Late Cretaceous. Described structure is a border of Pomeranian Swell (anticlinorium) and Szczecin Trough (synclinorium). Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-8)
Drawsko Pomorskie–Szubin fault zone
Basement fault zone with traces of reactivation in Mesozoic. (Country Report fault code: B-7)
Strefa uskoku podłoża ze śladami reaktywacji w mezozoiku. (Kod uskoku w Raporcie krajowym projektu HIKE: B-7)
Strefa uskokowa Rawsko Pomorskie–Szubin
Gryfice–Więcbork fault zone
Presumed basement fault controlling the extent of the Carboniferous and location of salt pillows. Method of observation: seismic profiles, gravimetry. Strike: WNW–ESE. (Country Report fault code: B-6)
Przypuszczalny uskok podłoża kontrolujący zasięg karbonu i usytuowanie poduszek solnych. Metoda obserwacji: profile sejsmiczne, grawimetria. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-6)
Strefa uskokowa Gryfice–Więcbork
Kujavian Swell (anticlinorium) is the middle part of the (NW-SE oriented) Mid-Polish Swell/anticlinorium, structurally deeper than its immediate NW (Pomeranian Swell segment) and SE counterparts.
Wyniesienie kujawskie jest częścią antyklinorium śródpolskiego, strukturalnie głębszą od przyległych od NW I SE.
Wyniesienie kujawskie
Kujavian Swell
Zgierz–Końskie fault zone
Probably Palaeozoic basement fault zone reactivated in the Mesozoic. Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-21)
Strefa uskokowa prawdopodobnie powstała w podłożu paleozoicznym, reaktywowana w mezozoiku. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-21)
Strefa uskokowa Zgierz–Końskie
Piotrków Trybunalski–Kłodawa–Bydgoszcz fault zone
Sigmoidalna strefa uskokowa mająca swoje korzenie w podłożu, reaktywowana w T3 – J1 jako strefa przesuwcza i w trakcie inwersji późnokredowej. Opisana struktura stanowi granicę wału kujawskiego i niecki łódzkiej. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE, N–S. (Kod uskoku w Raporcie krajowym projektu HIKE: B-14)
Strefa uskokowa Piotrków Trybunalski–Kłodawa–Bydgoszcz
Sigmoidal fault zone rooted in the basement, reactivated in the T3–J1 wrenching phase and during the Cr2 inversion phase. Described structure is a border of Kujavian Swell (anticlinorium) and Łódź Trough (synclinorium). Method of observation: seismic profiles. Strike: NW–SE, N–S. (Country Report fault code: B-14)
Brześć Kujawski–Kutno–Rawa Mazowiecka fault zone
Basement fault zone reactivated in the Mesozoic complex marked by the array of salt pillows and brachyanticlines partially teared out by faults. Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-13)
Strefa uskoków podłoża, reaktywowana w mezozoiku, gdzie wyznacza szereg poduszek solnych i brachyantyklin, częściowo poprzecinanych uskokami. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-13)
Strefa uskokowa Brześć Kujawski–Kutno–Rawa Mazowiecka
Sorgenfrei-Tornquist fault zone
Tectonic boundary interpreted from BABEL deep seismic experiment usually described as NW part of the TTZ (in Denmark and/or Sweden).
Granica tektoniczna interpretowana na podstawie głębokiego eksperymentu sejsmicznego BABEL, zwykle opisywana jako północno-zachodnia część TTZ (w Danii i / lub Szwecji).
Strefa Sorgenfrei'a-Tornquista
Sorgenfrei-Tornquist Zone
S-T fault zone 2
S-T fault zone 1
Szczecin Trough is an assymetric synclinorium bordering on the Fore-Sudetic homocline to the SW and the Mid-Polish Swell/anticlinorium (Pomeranian Swell) to the NE. Upper Palaeozoic and Mesozoic rocks form the backbone of this structure.
Niecka szczecińska od SW graniczy z monokliną przedsudecką, a od NE z antyklinorium środkowopolskim. Jest to struktura asymetryczna, zbudowana ze skał młodszego paleozoiku i mezozoiku.
Niecka szczecińska
Szczecin Trough
Drawno–Poznań fault zone
Reaktywowany na przełomie T3–J1 duży uskok podłoża, uruchamiający ciąg wysadów solnych ułożonych w ciąg typu en echelon (Szamotuły–Człopa); nieznacznie reaktywowany w Cr2. Opisywana struktura wyznacza granicę niecki szczecińskiej i łódzkiej. Metoda obserwacji: profile sejsmiczne. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-11)
Strefa uskokowa Drawno–Poznań
Major basement fault reactivated in T3–J1, creating en echelon array of salt diapirs (Szamotuły–Człopa), with minor reactivation in the Cr2. Described structure is a border of Szczecin Trough (synclinorium) and Łódź Trough (synclinorium). Method of observation: seismic profiles. Strike: NW–SE. (Country Report fault code: B-11)
Rostock–Szczecin fault zone
Limit of the zone of intense faulting in the Baltic region and a relatively more stable Gorzów Block to the SW, i.e. the border of Szczecin Trough (synclinorium) and Gorzów block. Method of observation: seismic profiles. Strike: WNW–ESE. (Country Report fault code: B-10)
Granica strefy pomiędzy intensywnie zuskokowanym rejonem bałtyckim i relatywnie stabilniejszym blokiem Gorzowa na SW, czyli granica niecki szczecińskiej i bloku Gorzowa. Metoda obserwacji: profile sejsmiczne. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-10)
Strefa uskokowa Rostock–Szczecin
Stralsund–Wolin fault zone
An array of en echelon faults in the Paleozoic basement and the Mesozoic cover. Method of observation: seismic profiles. Strike: WNW–ESE. (Country Report fault code: B-9)
Zespół uskoków typu en echelon, rozwinięty w podłożu paleozoicznym i pokrywie mezozoicznej. Metoda obserwacji: profile sejsmiczne. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: B-9)
Strefa uskokowa Stralsund–Wolin
Southern segment of the Trans-European Suture Zone
Southern part of the Trans-European suture zone (TESZ). TESZ is a litospheric-scale tectonic suture between the East European Craton and the Palaeozoic West European Platform.
Południowa część TESZ. TESZ to szew tektoniczny stanowiący granicę między kratonem wschodnioeuropejskim a platformą paleozoiczną Europy Zachodniej.
Południowa część strefy szwu transeuropejskiego
Puławy Trough
Niecka puławska należy do synklinoruym kościerzyńsko-puławskiego, leżącego po NE stronie wału środkowopolskiego.
Niecka puławska
Puławy Trough is the SE part of the Kościerzyna–Puławy synclinorium, bounding the Mid-Polish Swell/anticlinorium on the NE.
Iłża–Biłgoraj fault zone
The multi-stage fault zone at the boundary between two local domains: Radom–Kraśnik and Biłgoraj–Narol Blocks. It belongs to the TTZ (thus the edge of the EEC). The last significant phase of reactivation was in the end of the Cretaceous. Described structure is a border of Puławy Trough (synclinorium) and the Mid-Polish Swell (anticlinorium). Method of observation: seismic profiles, borehole data. Strike: NW–SE to WNW–ESE. (Country Report fault code: C-8)
Wielostopniowa strefa uskokowa na pograniczu dwóch jednostek lokalnych: bloków Radom–Kraśnik i Biłgoraj–Narol. Należy do strefy TTZ (a więc skraju kratonu wschodnioeuropejskiego). Ostatnia znacząca faza reaktywacji miała miejsce w końcu kredy. Strefa uskokowa Iłża–Biłgoraj stanowi granicę niecki puławskiej i wału środkowopolskiego. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: NW–SE do WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-8)
Strefa uskokowa Iłża–Biłgoraj
Southern region of the palaeozoic core of the Holy Cross Mountains, to the north limited by the Łysogóry thrust, to the south probably limited by the Lasocin–Strzelce fault zone that includes also the Chmielnik fault. Its northern sub-region, composed primarily of Devonian and Carboniferous rocks, is called the Kielce–Łagów synclinorium and its southern sub-region the Chęciny–Klimontów anticlinorium. The whole region is composed of Palaeozoic rocks of Lower Cambrian to Lower Carboniferous, deformed during the Caledonian and Variscan orogenies. Dense network of faults striking predominantly WNW–ESE, N–S and NNE–SSW cross-cuts it entirely. Caledonian deformation produced diabase and lamprophyre intrusions, Variscan deformations produced lamprophyres. Methods of observation: boreholes, geophysical data, geological maps, NMT, outcrops.
Południowy region w obrębie trzonu paleozoicznego Gór Świętokrzyskich, od północy ograniczony nasunięciem łysogórskim, a od południa najprawdopodobniej strefą uskokową Lasocin–Strzelce, w której skład wchodzi także uskok Chmielnika. Północna część regionu, zbudowana głównie ze skał dewońskich i karbońskich, określana jest jako subregion synklinorium kielecko-łagowskie, a południowa część jako subregion antyklinorium chęcińsko-klimontowskie. Region zbudowany jest ze zdeformowanych w trakcie orogenezy kaledońskiej i waryscyjskiej skał paleozoicznych od kambru starszego po karbon dolny. Region pocięty jest gęstą siecią uskoków o dominujących kierunkach WNW–ESE oraz N–S i NNE–SSE. Z ruchami kaledońskimi związane są intruzje diabazów i lamprofirów, a z ruchami waryscyjskimi związane są intrucje lamprofirów. Metody obserwacji: wiercenia, dane geofizyczne, mapy geologiczne, NMT, odsłonięcia.
Jednostka kielecka
Kielce tectonic domain
Dyminy fault zone
Fault zone overlapping a fold built of the Cambrian, Ordovician and Silurian rocks. It was subject to the main Caledonian activation phase and most likely Variscan reactivation of faults framing the structure from the N and the S. Method of observation: geological mapping, NMT, outcrops. Strike: E–W. (Country Report fault code: C-2)
Strefa uskokowa nasuwająca się na fałd zbudowany ze skał kambru, ordowiku i syluru. Główna faza aktywacji strefy uskokowej – kaledońska i, najprawdopodobniej, reaktywacja w czasie ruchów waryscyjskich uskoków otaczających strukturę od strony północnej i południowej. Metoda obserwacji: kartowanie geologiczne, NMT, odsłonięcia. Bieg: E–W. (Kod uskoku w Raporcie krajowym projektu HIKE: C-2)
Strefa uskokowa Dymin
Lasocin–Strzelce fault zone
Strefa uskokowa aktywna od dolnego paleozoiku do neogenu. Najbardziej intensywne deformacje miały miejsce w okresie waryscyjskim i alpejskim. Kinematyka uskoków była zmienna – od transtensji do transpresji. Opisywana struktura stanowi granicę między jednostką kielecką a blokiem małopolskim. Metody obserwacji: grawimetria, dane otworowe, kartowanie geologiczne, NMT, odsłonięcia. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-1)
Strefa uskokowa Lasocin–Strzelce
Multiple faults reactivated starting from the Lower Palaeozoic up to the Neogene. The most intense deformations during the Variscan and Alpine stages. Variable kinematics – from transtension to transpression. Described structure is a border of Kielce tectonic domain [pl: Jednostka Kielecka] and Małopolska Block. Method of observation: gravimetry, borehole data, geological Mapping, NMT, outcrops. Strike: NW–SE. (Country Report fault code: C-1)
Zbrza fault
High-angle reverse fault dipping to the SSW. Along it, the Palaeozoic and (partly) Mesozoic rocks are thrusted towards the NNE and the NE over the Mesozoic strata filling the Piotrkowice syncline. This fault is most probably a Variscan structure, intensly rejuvenated during the Alpine orogeny. Method of observation: gravimetry, borehole data, geological Mapping, NMT, outcrops. Strike: NW–SE. (Country Report fault code: C-1)
Wysokokątowy uskok odwrócony zapadający w kierunku SSW. Wzdłuż uskoku skały paleozoiczne i (częściowo) mezozoiczne przesuwane są w kierunku NNE i NE na warstwy mezozoiczne wypełniające synklinę Piotrkowicką. Uskok ten jest najprawdopodobniej strukturą waryscyjską, intensywnie odmładzaną podczas orogenezy alpejskiej. Metody obserwacji: grawimetria, dane otworowe, kartowanie geologiczne, NMT, odsłonięcia. Bieg: NW–SE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-1)
Uskok Zbrzy
Bardo fault zone
A zone of subparallel strike-slip faults with complex kinematics: from transtension (with igneous rocks intrusions) to transpression. The zone was formed during the Caledonian compressive stage. Described structure is a border of Kielce tectonic domain [pl: Jednostka Kielecka] and Carpathian Foredeep. Method of observation: gravimetry, borehole data, geological mapping, outcrops. Strike: WNW–ESE. (Country Report fault code: C-7)
Strefa równoległych uskoków przesuwczych o złożonej kinematyce: od transtensji (z intruzjami skał magmowych) do transpresji. Strefa powstała podczas kaledońskich ruchów kompresyjnych. Opisywana struktura stanowi granicę jednostki kieleckiej i zapadliska przedkarpackiego. Metody obserwacji: grawimetria, dane z otworów wiertniczych, kartografia geologiczna, wychodnie. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-7)
Strefa uskokowa Barda
Szydłówek fault zone
A series of thrusts directed towards the SSW and back-thrusts directed towards the NNE. Formed in the Variscan Late Carboniferous compressive stage. Along the frontal thrust, tectonically deformed Silurian and Lower Devonian rocks overlap the Upper Devonian rocks. Method of observation: gravimetry, borehole data, geological mapping, outcrops, NMT. Strike: E–W. (Country Report fault code: C-3)
Seria nasunięć w kierunku SSW i nasunięć wstecznych skierowanych ku NNE. Powstały w fazie kompresji waryscyjskiej, późnokarbońskiej. Wzdłuż czoła na skały górnego dewonu zachodzą tektonicznie zdeformowane skały syluru i dolnego dewonu. Metody obserwacji: grawimetria, dane z otworów wiertniczych, kartografia geologiczna, odsłonięcia, NMT. Bieg: E–W. (Kod uskoku w Raporcie krajowym projektu HIKE: C-3)
Strefa uskokowa Szydłówka
Szydłówek fault
Thrust to transpressive fault limiting the Szydłówek fault zone from the south. Along it Lower Palaeozoic (Silurian) and Lower Devonian rocks are thrusted over the Upper Devonian and Carboniferous rocks of Kielce syncline. The fault is a medium-angle structure dippig towards the N and NNE. Methods of observation: outcrops, boreholes, geologic map interpretation, NMT.
Uskok nasuwczy do transpresyjnego, ograniczjący od południa strefę uskokową Szydłówka. Wzdłuż jego powierzchni skały starszego paleozoiku (syluru) i starszego dewonu nasunięte są na skały dewonu młodszego i karbonu synkliny kieleckiej. Powierzchnia uskokowa zapada pod średnimi kątami w kierunku N i NNE. Metody obserwacji: odsłonięcia, wiercenia, interpretacja mapy geologicznej, NMT.
Uskok Szydłówka
Nida Trough
Niecka Nidy to południowo-wschodnia część synclinorium szczecińsko-miechowskiego, graniczącego z wałem środkowopolskim od SW.
Niecka nidziańska
Nida Trough (synclinorium) is the SE part of the Szczecin–Miechów synclinorium, bordering the Mid-Polish Swell (anticlinorium) on the SW.
Tarnów fault zone
A set of basement faults, reactivated in the Mesozoic and only slightly in the Miocene. It sets the trend of the large paleo-valley in the basement of the foredeep basin in front of the Carpathians. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: C-13)
Zespół uskoków podłoża reaktywowanych w mezozoiku i tylko nieznacznie w miocenie. Wyznacza trend dużej paleo-doliny w podłożu głębokiego basenu na przedpolu Karpat. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-13)
Strefa uskokowa Tarnowa
Bębica fault zone
A set of basement faults, reactivated in the Mesozoic and only slightly in the Miocene. It sets the trend of the large Pilsno paleo-valley in the basement of the foredeep basin in front of the Carpathians. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: C-13)
Zespół uskoków podłoża reaktywowanych w mezozoiku i tylko nieznacznie w miocenie. Wyznacza trend dużej paleo-doliny Pilzna w podłożu głębokiego basenu na przedpolu Karpat. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-13)
Strefa uskokowa Bębicy
Jędrzejów-Rzeszów fault set
A set of basement faults, reactivated in Mesozoic and only slightly in the Miocene. Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: C-12)
Zespół uskoków podłoża reaktywowanych w mezozoiku i tylko nieznacznie w miocenie. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-12)
Strefa uskokowa Jędrzejów–Rzeszów
Northern region of the Palaeozoic core of the Holy Cross Mountains, limited on the south by the Łysogóry thrust and on the north by the Skrzynna fault, composed of deformed Palaeozoic rocks of the Middle Cambrian to the Lower Carboniferous age. Structural style or this region is mostly due to the Variscan orogeny, but also arise, to some extent, from the Caledonian orogeny. The domain trends WNW–ESE and so do smaller sub-domains within it. Thrusts and transpression faults are located at the fronts of main folds whose limbs are thus displaced towards the SSW. This fold and thrust belt is criss-crossed by a dense network of high-angle, transverse (roughly N–S trending), strike-slip faults. Diabase intrusions into walls of tensional strike-slip faults are also related to Variscan displacements. Methods of observation: boreholes, geophysical data, geological maps, NMT, outcrops.
Północny region trzonu paleozoicznego Gór Świętokrzyskich. Od południa ograniczony nasunięciem łysogórskim, a od północy uskokiem Skrzynna. Budują go zdeformowane tektonicznie skały paleozoiczne od kambru środkowego po karbon dolny. Styl strukturalny zawdzięczją w głównej mierze orogenezie waryscyjskiej, a w mniejszym stopniu także orogenezie kaledońskiej. Przebieg jednostki to WNW–ESE, jednostki niższego rzędu posiadają taką samą orientację przestrzenną. U czoła głównych elementów fałdowych ulokowane są uskoki nasuwcze i transpresyjne, przemieszczające skrzydła nasuwane ku SSW. Całość przecięta jest gęstą siecią stromych, subpołudnikowych uskoków przesuwczych, poprzecznych do przebiegu jednostki. Z ruchami waryscyjskimi związane były intruzje diabazów ulokowane w skrzydłach tensyjnych uskoków przesuwczych. Metody obserwacji: wiercenia, dane geofizyczne, mapy geologiczne, NMT, odsłonięcia.
Jednostka Łysogórska
Łysogóry tectonic domain
Odrzywół–Jastrząb–Ćmielów Graben
Rów tektoniczny, odpowiednik rowu lubelskiego, ograniczający od N region świętokrzyski. Rów wypełniony jest osadami młodszego dewonu i karbonu. Od północy ogranicza go, równoległy do uskoku Skrzynna, uskok Nowe Miasto–Iłża–Bałtów. Rów powstał w wyniku ruchów waryscyjskich, a odmłodzony został w trakcie ruchów alpejskich. Metody obserwacji: geofizyka, wiercenia.
Rów Odrzywół–Jastrząb–Ćmielów
Tectonic graben which is a counterpart to the Lublin Trough (basin). It limits the Holy Cross region on the north and is filled with Late Devonian to Carboniferous sediments. Nowe Miasto–Iłża–Bałtów fault, parallel to the Skrzynna fault, limits it to the north. The Trough was formed during the Variscan orogeny and rejuvenated during the Alpine orogeny. Methods of observation: geophysics, borehole data.
Skrzynna fault
The northern border of the Łysogóry tectonic domain [pl: Jednostka Łysogórska] and the Holy Cross Mountains. The Skrzynna fault shows circa 1300 m of vertical displacement in the Palaeozoic rocks. The hypothetical SE continuation of this zone is the NE boundary of the Małopolska Massif. Methods of observation: gravimetry, seismic profiles, borehole data, geological mapping. Strike: WNW–ESE. (Country Report fault code: C-6)
Północna granica jednostki łysogórskiej i Gór Świętokrzyskich. Uskok Skrzynna wykazuje w skałach paleozoicznych około 1300 m przemieszczenia pionowego. Hipotetyczną kontynuacją tej strefy na SE jest północno-wschodnia granica bloku Małopolski. Metody obserwacji: grawimetria, profile sejsmiczne, dane otworowe, kartowanie geologiczne. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-6)
Uskok Skrzynnej
Rudki fault set
Horse-tail fault set formed due to the Variscan dextral strike slip. The eastern wall of this zone is displaced over 3 km towards the south. Pyrite and uranium deposits in Rudki are located in the tensive NE wing of the structure. Method of observation: borehole data, geological interpretation, NMT, outcrops. Strike: N–S. (Country Report fault code: SE part of C-5)
Zestaw uskoków o typie „końskiego ogona" utworzony w wyniku waryscyjskiego przesunięcia prawoskrętnego. Wschodnia część tej strefy jest przesunięta o ponad 3 km w kierunku południowym. Złoża pirytu i uranu w Rudkach znajdują się w NE skrzydle uskoku. Metody obserwacji: dane otworowe, interpretacja geologiczna, NMT, odsłonięcia. Bieg: N–S. (Kod uskoku w Raporcie krajowym projektu HIKE: SE część C-5)
Zespół uskoków Rudek
Rudki fault
Main fault of the Rudki fault set. It limits the horse-tail set from the west in its northern part and from the east in its southern part. The structure is a high-angle, ca. N–S oriented, right-lateral fault, transverse to the Łysogóry tectonic domain [pl: Jednostka Łysogórska] trend. This fault was formed during the Variscan orogeny, its northern region was probably rejuvenated during the Alpine orogeny. Methods of observation: boreholes, geologic map interpretation, NMT, outcrops.
Główny uskok w zespole uskoków Rudek. Ogranicza od zachodu strukturę typu koński ogon w jej północnej części, a od wschodu tą samą strukturę ale w jej południowej części. Jest to stromy, o południkowym przebiegu, prawoprzesuwczy uskok poprzeczny do przebiegu regionu łysogórskiego. Powstał w trakcie orogenezy waryscyjskiej. Prawdopodobnie jego N część odmłodzona w trakcie ruchów alpejskich. Metody obserwacji: otwory wiertnicze, interpretacja map geologicznych, NMT, odsłonięcia.
Uskok Rudek
Łysogóry fault zone
The overthrust of the folded Cambrian rocks of the Łysogóry tectonic domain [pl: Jednostka Łysogórska] onto the Lower Palaeozoic rocks of the Kielce tectonic domain [pl: Jednostka Kielecka]. Characterized by very low and low degree metamorphism. Multiple reactivation from the Lower Palaeozoic up to the Neogene. Its present trace at the surface is mostly due to the Variscan movements. Described structure is a border of Łysogóry and Kielce tectonic domains. Method of observation: gravimetry, geological mapping, NMT. Strike: WNW–ESE. (Country Report fault code: C-4)
Nasunięcie pofałdowanych skał kambru jednostki łysogórskiej na skały dolnego paleozoiku jednostki kieleckiej. Charakteryzuje się bardzo niskim i niskim stopniem metamorfizmu. Wielokrotna reaktywacja od dolnego paleozoiku do neogenu. Obecny ślad strefy uskoku łysogórskiego na powierzchni jest głównie wynikiem ruchów waryscyjskich. Opisana strefa stanowi rozdziela jednostkę łysogórską i kielecką. Metody obserwacji: grawimetria, kartografia geologiczna, NMT. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-4)
Strefa uskoku łysogórskiego
Małopolska Massif
Małopolska Massif (block) is composed of magmatic and metamorphic rocks of the Precambrian basement and the Palaeozoic sedimentary cover. The latter show hiatuses and angular discontinuities. The tectonic fabric of the block is a basin-and-range type of structure. It is located between the Upper Silesia block to the SW and the fold-and-thrust belt of the Holy Cross Mountains to the NE.
Masyw małopolski (blok małopolski) zbudowany jest z magmowych i metamorficznych skał podłoża prekambryjskiego I osadowych skał paleozoiku. W profilach utworów paleozoiku występują luki stratygraficzne (erozyjne) i niezgodności tektoniczne. Blok małopolski charakteryzuje się obecnością struktur zrębowych. Od SW sąsiaduje z blokiem górnośląskim, a od NE z pasmem fałdowym Gór Świętokrzyskich.
Masyw małopolski
Przedbórz–Przemyśl fault system
Its NW segment bounds heavily deformed Mesozoic surroundings of the Holy Cross Mts. from the SW. Its middle segment creates the SW edge of Precambrian core of the Małopolska Massif. Described structure is a border of the Małopolska Massif and the Miechów Trough (synclinorium). Method of observation: seismic profiles, borehole data. Strike: WNW–ESE. (Country Report fault code: C-11)
W NW części system uskoków ogranicza mocno zdeformowane SW mezozoiczne obrzeżenie Gór Świętokrzyskich. W środkowym odcinku tworzy południowo-zachodnią krawędź prekambryjskiego podłoża masywu małopolskiego. Opisana struktura stanowi granicę masywu małopolskiego i niecki miechowskiej. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: WNW–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-11)
System uskoków Przedbórz–Przemyśl
Ryszkowa–Wola fault zone
Old fault zone reactivated in the Miocene as a transpressive dextral zone rather than the transtensive sinistral one with minor displacement. Method of observation: seismic profiles, borehole data. Strike: NW–SE to WNW–ESE. (Country Report fault code: C-10)
Stara strefa uskokowa reaktywowana w miocenie bardziej jako transpresyjna strefa prawoprzesuwcza niż transtensyjna, z niewielkim przemieszczeniem. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: NW – SE do WNW – ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-10)
Strefa uskokowa Ryszkowa–Wola
Sandomierz–Lubaczów fault zone
Close to the Polish/Ukrainian border it is known as the Wielkie Oczy Graben which in fact is a half-graben downthrowing the SW wall by almost 1 km, in the Miocene. Method of observation: seismic profiles, borehole data. Strike: NW–SE to WNE–ESE. (Country Report fault code: C-9)
Niedaleko granicy polsko-ukraińskiej znany jest jako rów Wielkie Oczy, który w istocie jest pół-rowem zrzucającym w miocenie swoje południowo-zachodnie skrzydło o prawie 1 km. Metody obserwacji: profile sejsmiczne, dane z otworów wiertniczych. Bieg: NW–SE do WNE–ESE. (Kod uskoku w Raporcie krajowym projektu HIKE: C-9)
Strefa uskokowa Sandomierz–Lubaczów
Tectonic Boundary in Brandenburg
All named tectonic boundary objects that are located (at least partly) in Brandenburg, are identified by an ID with the prefix „DE-BB“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID. In addition, as the concepts are also located in Germany, they may have an additional ID in form of „DE“ referring to a national Germany-wide dataset.
Fault in Brandenburg displayed in the HIKE European fault database.
Fault Zones in the central part of the North German Basin
Störungszonen im Zentralteil des Norddeutschen Beckens
Fault zones in the central eastern part of the North German Basin (NGB) and the underlying basement. NGB : Intra-continental european basin, part of the Southern Permian Basin. Subsidence starting in Carboniferous. Inversion phases in Upper Cretaceous.
Störungszonen des zentralen östlichen Teiles des Norddeutschen Beckens und dessen basement. Norddeutsches Becken: Teil der Mitteleuropäischen Senke. Intrakontinentale Senkungsstruktur ab dem Karbon. Inversionsphasen in der Oberkreide.
Fault Zones of the central eastern North German Basin striking NNE-SSW
Störungszonen des zentralen östlichen Beckens, Streichen NNE-SSW
Fault zones and structure zones in the central eastern part of the North German Basin striking NNE-SSW.
Störungs- und Strukturzonen im östlichen Zentralbereich des Norddeutschen Beckens. Streichen NNE-SSW.
Rheinsberg Deep Fracture System
Rheinsberger Tiefenbruchsystem
Broad fault system striking NNE-SSW striking consisting of several parallel basement faults and related structures in the sedimentary cover. Reaching from the German Main Escarpments in the South (DE-BB-01a) to the Northern border of the NEGB. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics) and structures in the sedimentary cover (connected salt structures and related faults). Activation of Permian salt especially following the Kotzen-Zechlin structure zone.
NNE-SSW streichendes, breites Störungssystem im basement bestehend aus mehreren parallelen Störungszonen. Von den Mitteldeutschen Abbrüchen im Süden bis zur Nordgrenze der Norddeutschen Senke verlaufend. Postuliert basierend auf geophysikalischen Daten (Gravimetrie, Magnetik, tiefe Seismik) und Sekundärstrukturen im Deckgebirge. Aktivierung von Salztektonik insbesondere entlang der Kotzen-Zechliner Strukturzone.
Mirow Fault
Mirower Störung
NNE-SSW striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics).
NNE-SSE streichende Störung im basement. Postuliert nach geophysikalischen Befunden (Gravimetrie, Magnetik, Tiefe Seismik).
Kotzen-Zechlin Structural Zone
Kotzen-Zechliner Strukturzone
NNE-SSW and N-S striking structural zone in the sedimentary cover of the Rheinsberg Deep Fracture system. NNE-SSW and N-E elongted faults and salt anticlinals with several diapirs.
NNE-SSE und N-S streichende Strukturzone in jungpaläozoisch-mesozoischen Deckgebirge des Rheinsberger Tiefenbruchsystems. NNE-SSW und N-S orientierte Störungen und halokinetische Antiklinalstrukturen mit mehreren Diapiren.
Rheinsberg Fault
Rheinsberger Störung
NNE-SSE streichende Störung im basement . Postuliert nach geophysikalischen Befunden (Gravimetrie, Magnetik, Tiefe Seismik).
Neuruppin Fault
Neuruppiner Störung
NNE-SSE striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics).
Wredenhagen Fault
Wredenhagener Störung
NNE-SSW striking fault zone in the basement. Postulated. Activation of salt tectonics (salt structures Wredenhagen and Königsberg).
NNE-SSW streichende Störungszone im basement. Postuliert basierend auf geophysikalischen Daten und der Aktivierung von Salztektonik im Deckgebirge.
Arendsee Tiefenbruch
NNE-SSW striking basement fault zone. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics).
NNE-SSW streichende Störungszone im basement. Postuliert basierend auf geophysikalischen Daten (Gravimetrie, Magnetik, tiefe Seismik).
Dannenwalde Fault
Dannenwalder Störung
NNE-SSW striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics). In the Lower Permian Southeastern border of the Graben structure Zehdenick-Gransee-Graben.
NNE-SSW streichende Störungszone im basement. Postuliert basierend auf geophysikalischen Daten (Gravimetrie, Magnetik, tiefe Seismik). Im Rotliegend Südostgrenze der Grabenstruktur Zehdenick-Gransee.
Buckow-Oderhaff Fault Zone
Buckow-Oderhaff-Störungszone
NNE-SSW striking fault zone at the Eastern border of the NEGB. In the southern part (Buckow falt zone) reaching from the basement to the Cenozoic. In the Northern part (Oderhaff fault zone) only in the basement (postulated basing on geophysical data). Activation of salt tectonics along the fault zone.
NNE-SSW streichende Störungszone an der Östlichen Grenze der Norddeutschen Senke. Im südlichen Teil (Buckower Störungszone) vom basement bis in Känozoikum verfolgbar. Im nördlichen Teil (Oderhaff Störungszone) im basement (postuliert auf der Basis geophysikalischer Daten). Aktivierung von permischen Salz entlang der Störungszone.
Buckow Fault Zone
Buckower Störung
NNW-SSW striking fault zone reaching from the basement to the Cenozoic. Activation of salt tectonics along the fault zone (salt structures Buckow, Bad Freienwalde) . Sometimes interpreted as a extension of the Potsdam fault zone (DE-BB-02c-01).
NNW-SSE streichende Störungszone. Nachgewiesen vom basement bis ins Känozoikum. Aktivierung von Salztektonik entlang der Störungszone (Salzstrukturen Buckow, Bad Freienwalde). Teilweise interpretiert als östliche Verlängerung der Potsdamer Störungszone (DE-BB-02c-01).
Oderhaff Störungszone
NNE-SSW striking basement falt zone. Postulated basing on geophysical data. Postulated border between the Northeast German Basin and the Polish Trough.
NNE-SSE streichende Störung im basement. Postuliert nach geophysikalischen Befunden (Gravimetrie, Magnetik, Tiefe Seismik). Postulierte Grenze zwischen dem Norddeutschen Becken im Westen und dem Polnischen Becken im Osten.
Liebenwalde-Torgelow Fault
Liebenwalde-Torgelower Störung
Liebenwalde Fault
Liebenwalder Störung
Southwestern part of the Liebenwalde-Torgelow fault
Südlicher Teil der Liebenwalde-Torgelow-Störung
Fault Zones of the central eastern North German Basin striking WNW-ESE
Störungszonen des zentralen östlichen Beckens, Streichen WNW-ESE
Fault zones in the central eastern part of the North German Basin striking NW-SE and related fault sets especially in the Permocarboniferous.
Störungszonen im östlichen Zentralbereich des Norddeutschen Beckens und parallele Störungenscharen insbesondere im Permokarbon. Streichen NW-SE.
Templin Fault
Templiner Störung
NW-SE striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics). Active fault zone in the Carboniferous and Lower Permian (Rotliegend).
WNW-ESE streichende Störung im basement. Postuliert auf der Basis geophysikalischer Befunde (Gravimetrie, Magnetik, Tiefe Seismik). Aktive Störung im Karbon und Rotliegend.
Gramzow Fault
Gramzower Störung
WNW-ESE striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics).
WNW-ESE streichende Störung im basement. Postuliert auf der Basis geophysikalischer Befunde (Gravimetrie, Magnetik, Tiefe Seismik).
Schollene Störung
NW-SE striking fault in the Permocarboniferous.
NW-SE streichende Störung im Permokarbonen Deckgebirge.
Wittenburg Fault
Wittenburger Störung
NW-SE striking fault in the basement and the sedimentary cover. Defined basing on geophysical data (gravimetrics, magnetics, deep seismics) and faults in the Permocarboniferous.
NW-SE streichende Störung im basement und sedimentären Deckgebirge. Definiert nach geophysikalischen Befunden (Gravimetrie, Magnetik, Seismik) und Störungen im Permokarbon.
Havelberg Fault
Havelberger Störung
NW-SE striking basement fault with related structures in the sedimentary cover. Defined basing on geophysical data (gravimetrics, magnetics, deep seismics), faults in the Permocarboniferous.
NW-SE streichende Störung im basement und sedimentären Deckgebirge. Definiert auf der Basis geophysikalischer Befunde (Gravimetrie, Magnetik, Tiefe Seismik), Störungen im Permokarbon.
Teltow-Kotzen Fault
Teltow-Kotzener Störung
NW-ESE striking fault in the basement. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics). Active from Carboniferous to Triassic.
WNW-ESE streichende Störung im basement. Postuliert auf der Basis geophysikalischer Befunde (Gravimetrie, Magnetik, Tiefe Seismik). Aktive Störung von Karbon bis Trias.
Kotzen Fault
Kotzener Störung
Teltow Fault
Teltower Störung
Arneburg Fault
Arneburg Störung
NW-SE striking basement fault with related structures in the sedimentary cover. Defined basing on geophysical data (gravimetrics, magnetics, deep seismics), faults in the Permocarboniferous and salt structures.
NW-SE streichende Störung im basement und sedimentären Deckgebirge. Definiert auf der Basis geophysikalischer Befunde (Gravimetrie, Magnetik, Tiefe Seismik), Störungen im Permokarbon und halokinetischen Strukturen.
Falkensee Fault
Falkensee Störung
NW-SE striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics). Active from Carboniferous to Triassic.
Eberswalde Fault
Eberswalder Störung
NW-SE striking basement fault. Postulated basing on geophysical data (gravimetrics, magnetics, deep seismics).
Fault Zones of the central eastern North German Basin striking E-W
Störungszonen des zentralen östlichen Beckens, Streichen E-W
Complex fault zones in the central eastern part of the North German Basin striking approximately E-W.
Komplexe Störungszonen im östlichen Zentralbereich des Norddeutschen Beckens. Streichen in etwa E-W.
Potsdam Fault Zone
Potsdamer Störungszone
E-W striking, complex fault zone in the Permian and Mesozoic strata containing several faults and salt-cored anticlines. In some parts not exactly definable basing on the existing geophysical data (exploration gaps).
Komplexe, E-W streichende Strukturzone aus Störungen und halokinetischen Antiklinalstrukturen im Permischen und Mesozoischen Deckgebirge. Abschnittsweise bisher nicht exakt definierbar im geophysikalischen Bild (Erkundungslücken).
Lower Elbe Lineament - Barenthin Fault
Unterelbe Lineament - Barenthin fault
E-W striking basement structure (Lower Elbe Lineament). In the Permian to Mesozoic normal faulting and activation of several salt structures along the fault (Barenthin fault zone).
E-W streichende basement Struktur (Elbe Lineament). In der "Saxonischen" Tekonik im Perm und Mesozoikum normal faulting und Aktivierung von Salzstrukturen entland der Störung (Barenthin-Störungszone).
Fault Zones of the southern border of the North German Basin and Lausatian Block
Störungszonen des Südrandes des Norddeutschen Beckens und des Lausitzer Blockes
Fault zones of the Southeastern border of the North German Basin (NGB) and of the Variscian Lusatian Block. NGB : Intra-continental basin, part of the Southern Permian Basin. Subsidence starting in Carboniferous. Inversion phases in Upper Cretaceous. Lusatian Block: Variscian massif (consisting of Variscian and Cadomian intrusions, folded and low grade metamorphized sediments of the Rhenohercynian and Saxothuringian Zone), uplifted in Upper Cretaceous. Southern border of the NGB in Brandenburg.
Störungszonen der südöstlichen Grenze des Norddeutschen Beckens und des Variszischen Lausitzer Blocks. Norddeutsches Beckens: Teil der Mitteleuropäischen Senke. Intrakontinentale Senkungsstruktur ab den Karbon. Inversionsphasen in der Oberen Kreide. Lausitzer Block: in der Oberen Kreide angehobenes variszisches Massiv (cadomische und variszische Intrusionen, gefaltete und schwach metamorphisierte Sedimente der Rhenoherzynischen und Saxothuringischen Zone). Südliche Begrenzung des Norddeutschen Beckens in Brandenburg.
Variscian structures of the Lusatian Massif (Lusatian Anticline and the Torgau-Doberlug Syncline)
Variszische Strukturen des Lausitzer Massivs (Lausitzer Antiklinorium und Torgau-Doberlog-Synklinorium)
Variscian structure zones of the Lusatian Massif. Striking NE/ENE-SW/WSW. Partially re-activated during the different phases of the post-variscian development under varying stress regimes ("Saxonian" Tectonics from Permian to Tertiary).
Variszische Strukturzonen des Lausitzer Blockes. Streichen NE/ENE-SW/WSW. Teilweise reaktiviert in verschiedenen Phasen der post-variszischen Entwicklung ("Saxonische" Tektonik von Perm bis Tertiär) unter wechselnden Spannungsregimen.
South Doberlug Fracture Zone
Süd-Doberluger Bruchzone
Fault system at the southern border of the variscian Torgau-Doberlug Syncline, Variscian age. Striking NE-SW (Variscian).
Südliche Grenze der Variszischen Torgau-Doberlug-Synklinale. ENE-WSW streichende Störungszone.
Southern Doberlug Fracture Zone
Süd Doberluger Bruchzone
Finsterwalde Fault Zone
Finsterwalder Störungszone
Southern border of the Variscian Torgau-Doberlug Syncline, Variscian age. Striking ESE-WSW .
Südliche Grenze der variszischen Torgau-Doberlug-Senke. ESE-WSW streichende variszische Störung.
North Doberlug Fracture Zone
Nord-Doberluger Bruchzone
Northern border of Lusatian Massif to the Northeast German Basin (NEGB). Northern border of the Variscian Torgau-Doberlug Syncline. Striking ENE-WSW.
Nördliche Grenze des Lausitzer Blockes zur Norddeutschen Senke. Nördliche Grenze der Variszischen Torgau-Doberlug-Synklinale. ENE-WSW streichende Störingszone.
Central German Main Escarpments and parallel structures (Striking NW-SE)
Mitteldeutsche Abbrüche und Paralellstrukturen (Streichen NW-SE)
Faults zones at the Southeastern border of the North German Basin and related parallel structures striking NW-SE. Formed after the Variscian Orogeny as dextral strike-slip faults in a crustal wrench-system. Re-activated in different phases of the tectonic development of the NGB under varying stress regimes ("Saxonian" Tectonics from Permian to Tertiary). Extensional regimes with normal faulting from Jurassic to Early Cretaceous. Inversion in the Upper Cretaceous (forming of compression structures: thrusts, anticlines).
Störungszonen an der südöstlichen Grenze des Norddeutschen Beckens und Parallelstrukturen mit Streichen NW-SE. Bildung nach der Variszischen Orogenese als dextrale Scherzonen eines krustalen Wrench-Systems. Aktiviert in mehreren Phasen der tektonischen Entwicklung des Norddeutschen Beckens unter wechselnden Spannungsregimen ("Saxonische" Tektonik). Extensionsregime von Jura bis Unterer Kreide. Inversion in der Oberen Kreide (Bildung von Kompressionsstrukturen: Auf-/Überschiebungen, Antiklinalstrukturen).
Schönewalde Störung
NW-SE striking basement thrust of Variscian age. Reactivation during the Mesozoic "Saxonian" Tectonics. Vertical displacements up to 100m.
NW-SE streichende, variszische Krustenstörung. Reaktivierung in der in der mesozoischen "Saxonischen" Tektonik. Vertikale Versätze bis 100 m.
Zahna Störung
NW-SE striking fault in the foreland of the West Lusatian fault.
NW-SE streichende Störung im Vorland der Westlausitz-Störung.
Inter-Lusatian Fault
Innerlausitzer Störungszone
NW-SE striking fault zone of Variscian age. Reactivation during the Mesozoic "Saxonian" Tectonics.
NW-SE streichende variszische Störungszone. Reaktiviert in der in der "Saxonischen" Tektonik.
West Lusatian Fault
Westlausitzer Störungszone
NW-SE striking basement thrust of Variscian age. South-western border of the Lausation block. Reactivation during the Mesozoic "Saxonian" Tectonics.
NW-SE streichende variszische Krustenstörung. Südwest-Grenze des Lausitzer Blockes. Reaktivierung in der mesozoischen "Saxonischen" Tektonik.
Lusatian Main Escarpment
Lausitzer Hauptabbruch
The Lusatian Main Escarpment is one of the important basement thrusts at the Southeastern border of the North German Basin and forms the northeastern border of the Lusatian block to the NGB. Dextral strike-slip fault zone, striking NW-SE. Normal faulting in the Permian and Mesozoic with a vertical displacement up to more than 1.000m (decreasing from Southeast to Northwest). In the inversion phase in Upper Cretaceous with reverse faulting.
Der Lausitzer Haupptabbruch ist eine der wichtigen Krustenstörungen am Südrand der Norddeutschen Senke und bildet die nordöstliche Grenze des Lausitzer Blockes zur Norddeutschen Senke. Dextrale strike-slip-Störung mit Abschiebungsbewegungen im Perm und Mesozoikum mit vertikalen Versätzen bis zu 1000m (von Südost nach Nordwest abnehmend). Während der Inversion in der Oberen Kreide mit Rücküberschiebungen.
Wünsdorf-Cottbus Fault
Wünsdorf-Cottbus Störung
NW-SE striking fault zone in the basement and sedimentary cover. In the sedimentary cover partially as a flexure. Especially in the northern part characteristic strong gradients of the Bouguer anomaly ("Wünsdorf-Cottbusser gravity flank").
NW-SE streichend Störungszone im basement und Deckgebirge. Im Deckgebirge teilweise als Flexur ausgebildet. Insbesondere im nördlichen Teil markante Anomalien der Bouguerschwere ("Wünsdorf-Cottbusser Schwereflanke").
Groß Köris-Dissen-Merzdorf Fault Zone
Groß-Köris - Dissen - Merzdorfer Störungszone
NW-SE striking fault zone in the basement and overburden. Dextral strike-slipe fault. Formation of elongated salt-cored anticlines during the compression phases in Upper Cretaceous.
NW-SE streichend Störungszone im basement und Deckgebirge. Dextrale strike-slip-Störung. Durch Kompressionsphasen in der Oberen Kreide Bildung von Antiklinal-Strukturen im permo-triassichen Deckgebirge, mit langestreckten Salzstrukturen im Kern.
Groß Köris-Merzdorf Structural Zone
Groß Köris-Merzdorfer Strukturzone
Dissen-Merzdorf Fault Zone
Dissen-Derzdorfer Störungszone
Fürstenwalde-Guben Structural Zone
Guben-Fürstenwalder-Störungszone
NW/NNW-SE/SSE striking fault zone in the basement and sedimentary cover. Complex system of fracture zones, Graben structures and salt-cored anticlines.
NW-SE bis NNW-SSE streichende Störungszone im Deckgebirge und basement. Komplexes Störungsbild aus Bruchstrukturen, antiklinalen Elementen und Salzstrukturen.
Fürstenwalde Fault Zone
Fürstenwalder Störungszone
Guben Fault Zone
Gubener Störungszone
Vetschau Fault
Vetschauer Störung
NW-SE striking fault zone in the sedimentary cover between Lusatian Main Escarpmenmt and Wünsdorf-Cottbus fault.
NW-SE streichende Störungszone im Deckgebirge zwischen Lausitzer Abbruch und Wünsdorf-Cottbuser Störungszone.
Kausche Graben
Kauscher Graben
Cenozoic Graben structure in the forland of the Lusatian Main Escarpment. Vertical displacement some decameter.
Känozoische Grabenstruktur im Vorland des Lausitzer Hauptabbruches. Vertikale Versätze von einigen 10er Metern.
Schweinitz Störung
Zerben-Belzig Structural Zone
Zerben-Belzig Strukturzone
NW-SE striking structural zone. Elongated faulted anticlinale with accumulation of Zechstein salt in the core (thicknes > 1000m).
NW-SE streichende Strukturzone. Langestreckte gestörte Antiklinalkstruktur mit Akkumulation von Zechstein-Salz im Kern (bis 1500 m Mächtigkeit).
Setzsteig Structural Zone
Setzsteiger Strukturzone
NW-SE striking fault zone. Reverse fault in the basement (vertical displacement up to 1000 m) and a salt-cored anticline in the sedimentary cover (Reuden-Setzsteig).
NW-SE streichende Störungszone. Aufschiebung im basement mit vertikalem Versatz bis 1000m. Aufsitzende Salzstruktur Reuden-Setzsteig im Deckgebirge.
Burg-Reuden Störung
Part of the Setzsteig structural zone.
Teil der Setzsteiger Strukturzone
Cross-directional structures of the Central German Main Escarpments (Striking NE-SW)
Querstrukturen der Mitteldeutschen Abbrüche (Streichen SW-NE)
Fault and fracture zones at the Southern border of the North German Basin striking cross-directional to the Central German main escarpments (SW/WSW-NE/ENE). Post-variscian origin ("Saxonian" Tectonics from Permian to Tertiary). Partially re-activation of Variscian structures.
Saxonische Störungs- und Bruchzonen an der südöstlichen Grenze des Norddeutschen Beckens. Streichen quer zu den Mitteldeutschen Abbrüchen (SW/WSW-NE/ENE). Bildung post-variszisch ("Saxonische" Tektonik). Teilweise Reaktivierung variszischer Strukturen.
Hoyerswerda Fault
Hoyerswerdaer Querstörung
NE-SW striking fault zone of the "Saxonian" Tectonics.
NE-SW streichende Störungszone der "Saxonischen" Tektonik.
Hoyerwerdaer Querstörung
Stradow-Buckow Fault
Stradow-Buckower Störung
Herzberg Fault Zone
Herzberger Störung
Calau-Plieskendorf-Buchwäldchen Fault Zone
Calau-Plieskendorfer Störungszone
NE-SW striking fault zone of the "Saxonian" Tectonics. Vertical displacement influenced by fault-controlled subrosion of Permian salt.
NE-SW streichende Störungszone der "Saxonischen" Tektonik. Vertikale Bewegungen durch störungskontrollierte Subrosion von Permischen Salz beeinflusst.
Calau Fault
Calauer Störung
Plieskendorf Fault
Plieskendorfer Störung
Heinersbrück-Guben Fault Zone
Heinersbrück-Gubener Störungszone
Heinersbrück Fault
Heinersbrücker Störung
Senftenberg Fault
Senftenberger Störung
Heinersbrück-Guben Fault
Heinersbrück-Gubener Querstörung
Bronkow-Tauer Fault Zone
Bruchzone Bronkow-Tauer
Bronkow Fault
Bronkower Störung
Tauer-Pinnow Fault
Tauer-Pinnow Störungszone
Fracture Zones of the Northeastern border of the North German Basin
Störungszonen des Nordrandes des Norddeutschen Beckens
Fault zones of the Eastern/Northeastern border of the North German Basin (NGB). NGB : Intra-continental european basin, part of the Southern Permian Basin. Subsidence starting in Carboniferous. Inversion phases in Upper Cretaceous.
Störungszonen des östlichen/nordöstlichen Randes des Norddeutschen Beckens. Norddeutsches Becken: Teil der Mitteleuropäischen Senke. Intrakontinentale Senkungsstruktur ab den Karbon. Inversionsphasen in der Oberkreide.
Fault Zones Zones of the Northeastern border of the North German Basin striking NNW-SSE
Störungszonen des nordöstlichen Randes des Norddeutschen Beckens, Streichen NNW-SSE
NNW-SSE striking fault zones at the Northeastern border of the North German Basin. Southern extension of the Western Pommerania Fault system.
NNW-SSE streichende Störungszonen am Nordrand des Norddeutschen Beckens. Südliche Ausläufer des Vorpommern-Störungssystem.
All named tectonic boundary objects that are located (at least partly) in the Netherlands, are identified by an ID with the prefix „NL“ listed in the notation. Fault systems and/or fault domains can cross political borders and are therefore shared by several countries. Therefore, they can contain faults from different countries, indicated by country-specific prefixes to the respective ID.
Fault in the Netherlands displayed in the HIKE European fault database. They are sorted into fault systems and tectonic terranes (Fault Domains) represented in the Geological Map of the Netherlands and Dutch subsurface geological models DGM (v2.2) and DGm diep (v5).
Tectonic Boundary in the Netherlands
The exact position of this terrane depends on its definition. In the most recent views it corresponds to a Low Velocity Zone in the crust that is attributed to the Caledonian accretionary wedge inbetween Avalonia and Baltica that formed due to Thornquist ocean subduction and is attached to non-subducting Avalonia plate. This definition places the Tor suture south of this accretionary terrane, wheras the deeper seated plate contact might be represented by the Elbe-Line. However, it would be unfortunate to reposition the Thor suture which is positioned further north and likely represents the northern suture of the accretionary prism
Caledonian Accretionary complex
collapsed Caledonian accretionary Complex
Thor accretionary wedge
Caledonian Accretionary Terrane Fault Domain
CAT-FD
Group of faults associated with the approximately N-S trending part of the Dutch Central Graben and its surroundings in the northernmost Dutch offshore
Northern Dutch Offshore Graben Large Scale Fault System
NDOG-LSFS
Faults associated with the N-S trending Dutch Central Graben system
Dutch Central Graben Fault System
DCG-FS
N-S trending fault system acting as the eastern margin fault system of the Dutch Central Graben
Eastern Dutch Central Graben Boundary sub Fault System
E-DCGB-sFS
N-S trending fault system acting as the western margin fault system of the Dutch Central Graben
Western Dutch Central Graben Boundary sub Fault System
W-DCGB-sFS
Undifferentiated faults within the Dutch Central Graben
Intra Dutch Central Graben Fault Domain
DCG-FD
Undifferentiated faults above the Zechstein Group within the Dutch Central Graben
Dutch Central Graben supra-salt Fault Domain
DCG-SUPRA-FD
Undifferentiated faults below the Zechstein Group within the Dutch Central Graben
Dutch Central Graben sub-salt Fault Domain
DCG-SUB-FD
Undifferentiated faults within the Step Graben. Predominantly N-S oriented faults have been observed, but interpretation density is limited in this area
Intra Step Graben Fault Domain
SG-FD
Undifferentiated faults above the Zechstein Group within the Step Graben
Step Graben supra-salt Fault Domain
SG-SUPRA-FD
Undifferentiated faults below the Zechstein Group within the Step Graben
Step Graben sub-salt Fault Domain
SG-SUB-FD
Aligned system of N-S faults defining the northernmost narrowing part of the Step Graben, i.e. at the transition to the Outer Rough Basin in Germany and Denmark
Outer Rough Basin sub Fault System
ORB-sFS
This fault system separates the Step Graben from the Elbow Spit Platform and Elbow Spit High
Step Graben Boundary Fault System
SGB-FS
Undifferentiated faults within the Elbow Spit Platform
Intra Elbow Spit Platform Fault Domain
ESP-FD
NNW-SSE trending fault system in between the Step Graben and the Elbow Spit Platform
Elbow Spit Platform Margin Fault System
ESPM-FS
Elbe Line
Deep-seated plate contact betwen Avalonia and Baltica underneath the Thor accretionary wedge, situated close to the northern offshore border with Germany. The line is rather hypothetical in the sense that it cannot be seen at shallow levels where most faults are normally interpreted
The Brabant Massif is currently considered to be situated above the boundary of two lithospheric blocks, the Midlands Microcraton to the SW and the Southern North Sea - Lüneberg Terrane to the NE and formed during final closure of the Rheic ocean between Laurentia and Gondwana. the Welsh basin - London-Brabant massif forms a stable block together with the Midlands micro-craton (UK). Two distinct fault directions occur in this domain, i.e.,WNW-ESE and NNW-SSE trending. The latter group is less developed in the Netherlands.
Wales-Brabant Massive Fault Domain
London-Brabant Massief
WBM-FD
Brabant Massief
Group of predominantly WNW-ESE faults in the Northeastern flank of the Brabant Massif that is covered by Paleozoic to Triassic strata, which in turn are unconformably overlain by Upper Cretaceous strata. The southern boundary of the Campine Basin is defined as the area where Carboniferous rocks pinch out or are locally delimited by faults (e.g. the Hoogstraten syn-depositional fault). Faults part of the Campine block have common activity during the Kimmerian and/or Cenozoic tectonic phases.
Campine Block Fault Domain
Campine Basin
CAM-FD
Kempen Blok
A relatively unfaulted area in the Campine Block that acted as depocenter (subsidence area) and was formed due to flexural downwarping in response to Paleogene inversion of the West Netherlands Basin to the north
Voorne trog Fault Domain
VT-FD
Boundary fault between the Oosterhout Platform and the Campine basin
Northern Zeeland Fault System
N-ZL-FS
Faults in the area south of the Southern West Netherlands Basin sub Fault System that form a transitional area between the Roer Valley Graben in the north and the Zeeland High (or Campine Block) in the south. Here, Triassic rocks are preserved and unconformably overlain by Upper Cretaceous. The southern boundary of the Oosterhout Platform is defined as the area where Triassic rocks pinch out and is only locally defined by faults
Oosterhout Platform Fault Domain
OP-FD
WNW-ESE trending major normal, listric fault within the Campine block probably active during the Carboniferous based as is based on roll-over anticlines in Namurian and Westphalian strata that are unconformably overlain by Cretaceous deposts. It defines the southern extent of Upper Carboniferous rocks. It is only mapped just south of the Netherlands-Belgium border.
Hoogstraten Fault System
HS-FS
Group of predominantly WNW-ESE faults normal/oblique faults in the Limburg High, which is the southeasternmost extension of the Zeeland-Kempen-Limburg Fault Domain. In this area, Upper Cretaceous deposits directly overlie Carboniferous rocks. In the south, east and west, the Limburg High gives way to the adjacent fault blocks in Germany and Belgium.
Limburg High Fault Domain
LH-FD
Group of predominantly WNW-ESE faults normal/oblique faults in the Zeeland Province part of the Wales Brabant massive that is characterized by Upper Cretaceous rocks directly overlying Carboniferous rocks. It is bounded in the north by the Oosterhout Platform, where Triassic rocks are found.
Zeeland High Fault Domain
ZH-FD
Faults formed in that part of the Avalonia micro plate that was extended and collapsed in latest Devonian-earliest Carboinferous time at the onset of the Variscan orogeny and that were reactivated during younger deformation phases . The fault domain is separated form the southern part of Avalonia through the Dowsing-South Hewett fault zone
Southern North Sea Lüneberg Fault Domain
SNSL-FD
Mid Netherlands Basins Fault Domain
A structural domain defined by the area south of the Dutch Central Graben and Platform fault domains in the north and delimited by the Dowsing-South Hewett Fault System to the south. It consists of several NW-SE and WNW-ESE basin systems that are separated by major normal and reverse faults
CNB-LFS
Basin system with multiple internal faults that were active during Kimmerian, Subhercynian and/or Cenozoïc tectonic phases. The characteristics of the Jurassic subsidence pattern reveal that the Roer-Valley Graben and West Netherlands Basin formed a single tectonic unity during the Mesozoic, but it probably already existed as a structural feature in Paleozoic times that was formed due to wrench movements after the Late Carboniferous–Early Permian Variscan orogeny
Roer-Valley Graben - West Netherlands Basin Fault Domain
RVG-WNB-FD
The Roer Valley Graben (RVG) is a distinct fault-bounded graben with multiple internal faults of predominantly NNW-SSE orientations and some NW-SE orientations. Faults were active during Kimmerian, subhercynian and/or Cenozoïc tectonic phases, but it is since the Jurassic that differential subsidence clearly started. Since the Early Cretaceous rocks are missing in the RVG, it is not clear which tectonic regime the RVG experienced in those times. subsidence recommenced in Oligocene times and continues to the present day. Apart from the northwest, where the RVG passes into the West Netherlands Basin (WNB), it is surrounded by platform areas. The boundary to the WNB has been taken at the pinch-out line of Upper Cretaceous sediments. Paleogene uplift of the RVG was less severe than in the WNB, and pre-inversion Chalk has been preserved in the RVG. The northeastern boundary of the basin isformed by the Peel Boundary Fault System
Roer-Valley Graben Fault Domain
RVG-FD
Indefetigable Platform formes the domain west of the West Netherlands Basin and BFB. The southern part is also referred to as Winterton Platform
Indefetigable Platform Fault Domain
IDP-FD
Indefetigable Shelf
The Winterton High is part of the Indefetigable Platform Fault Domain and is charaterized by the absence of Permian and Mezozoic strata
Winterton High sub Fault Domain
WH-sFD
The West Netherlands Basin (WNB) is a Mesozoic distinct fault-bounded graben with multiple internal faults of predominantly NNW-SSE and NW-SE orientations that toghether make up an anastomosing fault mosaic. The basin which was mildly- to strongly inverted in Late Cretaceous and Paleogene times. The southeastern transition toward the Roer Valley Graben (RVG) corresponds to the area where the Chalk has been completely eroded due to inversion. In the southwest, the Sout West Netherlands Fault System marks the boundary to the Campine Block or Oosterhout Platform. The transition towards the Indefatigable Platform is irregular and runs across different fault blocks. In the northeast, the boundary with the Broad Fourteens- and Central Netherlands basins is formed by the North West Netherlands Fault System, which more or less coincides with the narrow Zandvoort Ridge and IJmuiden Platform
West Netherlands Basin Fault Domain
WNB_FD
NNW oriented fault system active during Paleocene -(sub)Recent times and that has acted as the local boundary to the RVG since Cenozoic times. During the Mesozoic the main step fault was at the Southern West Netherlands Basin Fault System
Rijen Fault System
RIJN-FS
Gilze-Rijen Breuk
Group of faults transecting the WNW-ESE elongated structural High delimited to the south by the Peel - Indefatigable Large Scale Fault System
Peel - Maasbommel_Zandvoort Fault Domain
PMZ-FD
Undifferentiated faults within the Peel Maas Bommel Complex
Peel Maas Bommel Complex Fault Domain
PMBC-FD
The northern margin fault of the Peel Maas Bommel High
Tegelen Fault System
TEG-FS
Fault block between Central Netherlands Basin and West Netherlands Basin defined by severe faulting along WNW-ESE faults. This structure is an important inversion ridge, locally accompanied by southvergent reverse- and thrust faults
Zandvoort Ridge Fault Set
ZR-FSET
Fault within the a mild inversion structure just offshore IJmuiden dilimited to the south by the Indefatigable Fault System
IJmuiden Platform Fault Domain
IJP-FD
NW-SE alignment of the Peel Boundary, Mid-Netherlands and Indefatigable Fault system that make up the northern boundary of the Roer-Valley Graben - West Netherlands Basin Fault Domain
Peel - Indefatigable Large Scale Fault System
P-ID-LFS
Alignment of NW-SE faults that form the transition between the Peel Maasbommel High in the north and the Roer Valley Graben in the south
Peel Boundary Fault System
PB-FS
Alignment of NW-SE faults that form the transition between the Zandvoort Ridge to the north and the West Netherlands Basin to the south. The Mid Netherland Fault System acted as reverse faults during inversion
Mid Netherland Fault System
MN-FS
Alignment of NW-SE faults that form the transition between the Broad Fourteens Basin to the north and the West Netherlands Basin to the south. Locally, the Mid Netherland Fault System acted as reverse faults during inversion
Indefatigable Fault System
ID-FS
Faults associated with the NW-SE aligned basin system in the central Netherlands
Central Netherlands - Broad Fourteens Fault Domain
CNB-BFB-FD
Undifferentiated faults within Central Netherlands Basin
North Holland Platform Fault Domain
NHP_FD
Complex Fault patterns forming the eastern Boundary of the North Holland platform
North Holland Platform Fault System
NHP-FS
Internal Broad Fourteens Basin Fault System
I-BFB-FS
Northern Central Netherlands Basin Fault System
Complex Fault patterns forming the Boundary between the Central Netherlands Basin and the Peel Maas Bommel Complex in the west and bifurcating from the Southern Central Netherlands Fault System towards the Northeast
N-CNB-FS
Complex Fault patterns forming the western Boundary of the Broad Fourteens Basin
Western Broad Fourteens Basin Fault System
W-BFB-FS
Complex Fault patterns forming the eastern Boundary of the Broad Fourteens Basin
Eastern Broad Fourteens Basin Fault System
E-BFS-FS
Complex Fault patterns forming the Boundary between the Central Netherlands Basin and the Peel Maas Bommel Complex
S-CNB-FS
Southern Central Netherlands Basin Fault System
Undifferentiated faults within Broad Fourteens Basin
Broad Fourteens Basin Fault Domain
BFB-FD
Central Netherlands Basin Fault Domain
CNB-FD
A structural domain largely defined by the area southwest of the Dutch Central Graben
Western Dutch Platform Fault Domain
WDP-FD
Group of faults within the Central offshore Platform that is seen as the transitional zone between the Dutch Central Graben and the Broad Fourteen Basin
Intra Central Offshore Platform Fault Domain
COP-FD
Faults with a NNW-SSE orietation below the Zechstein Group within the Central Offshore Platform
Central Offshore Platform sub-salt NNW-SSE Fault Set
COP-SUB-NNW-SSE-FSET
Undifferentiated faults above the Zechstein Group within the Central Offshore Platform
Central Offshore Platform Supra-salt Fault Domain
COP-SUPRA-FD
Faults with a NNE-SSW orietation below the Zechstein Group within the Central Offshore Platform
Central Offshore Platform sub-salt NNE-SSW Fault Set
COP-SUB-NNE-SSW-FSET
Faults with a WSW-ENE orietation below the Zechstein Group within the Central Offshore Platform
Central Offshore Platform sub-salt WSW-ENE Fault Set
COP-SUB-WSW-ENE-FSET
Faults with a WNW-ESE orietation below the Zechstein Group within the Central Offshore Platform
Central Offshore Platform sub-salt WNW-ESE Fault Set
COP-SUB-WNW-ESE-FSET
NNE-SSW oriended fault system acting as the transition zone between Texel-IJsselmeer High in the east and the Central Offshore Platform in the west
Central Offshore Platform Margin Fault System
COPM-FS
Group of faults with various orientations within the Cleaver Bank
Intra Cleaver Bank Fault Domain
CB-FD
Faults with a WSW-ENE orietation below the Zechstein Group within the Cleaver Bank
Cleaver Bank sub-salt WSW-ENE Fault Set
CB-SUB-WSW-ENE-FSET
Faults with a WNW-ESE orietation below the Zechstein Group within the Cleaver Bank
Cleaver Bank sub-salt WNW-ESE Fault Set
CB-SUB-WNW-ESE-FSET
Faults with a NNW-SSE orietation below the Zechstein Group within the Cleaver Bank
Cleaver Bank sub-salt NNW-SSE Fault Set
CB-SUB-NNW-SSE-FSET
Undifferentiated faults above the Zechstein Group within the Cleaver Bank
Cleaver Bank Supra-salt Fault Domain
CB-SUPRA-FD
Faults with a NNE-SSW orietation below the Zechstein Group within the Cleaver Bank
Cleaver Bank sub-salt NNE-SSW Fault Set
CB-SUB-NNE-SSW-FSET
Fault system defining the eastern margin of the Cleaver Bank
Eastern Cleaver Bank Margin Fault System
E-CBM-FS
Fault system defining the northern margin of the Cleaver Bank
Northern Cleaver Bank Margin Fault System
N-CBM-FS
Group of faults with various orientations within Anglo-Dutch Basin
Intra Anglo-Dutch Basin Fault Domain
ADB-FD
Undifferentiated faults above the Zechstein Group within the Anglo-Dutch Basin
ADB Supra-salt Fault Domain
ADB-SUPRA-FD
Faults with a NNE-SSW orietation below the Zechstein Group within the Anglo-Dutch Basin
ADB sub-salt NNE-SSW Fault Set
ADB-SUB-NNE-SSW-FSET
Faults with a WSW-ENE orietation below the Zechstein Group within the Anglo-Dutch Basin
ADB sub-salt WSW-ENE Fault Set
ADB-SUB-WSW-ENE-FSET
Faults with a WNW-ESE orietation below the Zechstein Group within the Anglo-Dutch Basin
ADB sub-salt WNW-ESE Fault Set
ADB-SUB-WNW-ESE-FSET
Faults with a NNW-SSE orietation below the Zechstein Group within the Anglo-Dutch Basin
ADB sub-salt NNW-SSE Fault Set
ADB-SUB-NNW-SSE-FSET
A structural domain largely defined by the area east of the Dutch Central Graben
Eastern Dutch Platform Fault Domain
EDP-FD
Faults within the Terschelling Basin
Intra Terschelling Basin Fault Domain
TB-FD
Undifferentiated faults above the Zechstein Group within the Terschelling Basin
Terschelling Basin supra-salt Fault Domain
TB-SUPRA-FD
Undifferentiated faults below the Zechstein Group within the Terschelling Basin
Terschelling Basin sub-salt Fault Domain
TB-SUB-FD
Group of fault within the Ameland Platform that is partly delimited to the east by the Western Lauwerszee Trough Fault System
Intra Ameland Platform Fault Domain
AP-FD
Faults with a N-S W orietation below the Zechstein Group within the Ameland Platform
Ameland Platform sub-salt NNW-SSE Fault Set
AP-SUB-NNW-SSE-FSET
Faults above the Zechstein Group with predominantly NW-SE and WNW-ESE orientation within the Ameland Platform
Ameland Platform supra-salt Fault Domain
AP-SUPRA-FD
Faults with a NNE-SSW orietation below the Zechstein Group within the Ameland Platform
Ameland Platform Platform sub-salt NNE-SSW Fault Set
APP-SUB-NNE-SSW-FSET
Faults with a WSW-ENE orietation below the Zechstein Group within the Ameland Platform
Ameland Platform Platform sub-salt WSW-ENE Fault Set
AP-SUB-WSW-ENE-FSET
Faults with a WNW-ESE orietation below the Zechstein Group within the Ameland Platform
Ameland Platform sub-salt WNW-ESE Fault Set
AP-SUB-WNW-ESE-FSET
Alignment of NW-SE faults and structural blocks defining the
Texel-Ijsselmeer High Fault System
TIJH-FS
In the western part of the Netherlands, the Texel-IJsselmeer Fault System is the northernmost marginal fault of the Texel-IJsselmeer High
Northern Texel-Ijsselmeer High sub Fault System
N-TIJHM-SFS
Undifferentiated faults within the Texel-IJsselmeer High
Intra Texel IJsselmeer Fault Domain
TIJM-FD
In the western part of the Netherlands, the Texel-IJsselmeer Fault System is the southernmost marginal fault of the Texel-IJsselmeer High
Southern Texel-Ijsselmeer High sub Fault System
S-TIJHM-SFS
A group of faults within the Friesland Platform that define the Vlieland Basin
Vlieland Basin Fault Domain
VB-FS
Faults within the Vlieland Basin
Intra Vlieland Basin Fault Domain
VB-FD
Undifferentiated faults above the Zechstein Group within the Vlieland Basin
Vlieland Basin supra-salt Fault Domain
VB-SUPRA-FD
Undifferentiated faults below the Zechstein Group within the Vlieland Basin
Vlieland Basin sub-salt Fault Domain
VB-SUB-FD
The southern marginal fault system of the Vlieland Basin that together with the Texel-IJsselmeer High Fault System forms a step-like transition to the Texel-IJsselmeer High
Southern Vlieland Basin Boundary Fault System
S-VB-SFS
Undifferentiated faults within the Groningen Platform that forms the eastern block to the east of the Lauwerzee Trough and delimits the Lower Saxony Basin to the North. It continues offshore into the area defined as Dutch-German G&L Platform Fault Set
Groningen Platform Fault Domain
GP-FD
Undifferentiated faults above the Zechstein Group within Groningen Platform
Groningen Platform supra-salt Fault Domain
GP-SUPRA-FD
A complex fault pattern with 4 main fault groups at Rotliegend- and deeper stratigraphic levels that can related to at least three phases of deformtation since Paleozoic times. Early Carbinferous carbonate platforms are generally bounded by NE-SE faults supporing the notion that these are lon-leved Paleozoic structures. The lack of similarly faulted Rotliegend outcrop analogues and the fact that these strain features can thus only be studied in seismic data leaves room for multiple interpretations
Groningen Platform sub-salt Fault Domain
GP-SUB-FD
A complex amalgamation of differently oriented faults making up the transistion between the Groningen Platform and the Lauwerzee Trough. This fault system post dates the NW-SE faults in the area and is of Mesozoic age.
Eastern Lauwerzee Trough Fault System
ELZT_FS
Group of faults with various orientations within the Schilgrund Platform
Intra Schill Grund Platform Fault Domain
SGP-FD
Undifferentiated faults above the Zechstein Group within the Schilgrund Platform
Schill Grund Platform supra-salt FaultDomain
SGP-SUPRA-FD
Undifferentiated faults below the Zechstein Group within the Schilgrund Platform
Schill Grund Platform sub-salt Fault Domain
SGP-SUB-FD
Western Lauwerzee Trough Fault System
WLZT-FS
Southern boundary fault zone to the Schilgrund Platform
Rif Gronden Fault System
RG-FS
Undifferentiated faults within the Lower Saxony Basin
Lower Saxony basin Fault Domain
LSB_FD
Aligned NNW-SSE faults in the offshore blocks G and L north of (and part of) the Groningen Platform that continues accros the border with Germany
G and L Platform Fault Set
GLP-FSET
Faults above the Zechstein Group with predominantly NW-SE and WNW-ESE orientation within the G&L Platform
G en L Platform Supra-salt Fault Domain
GLP-SUPRA-FD
Faults with a NNE-SSW orietation below the Zechstein Group within the G&L Platform
G en L Platform sub-salt NNE-SSW Fault Set
GLP-SUB-NNE-SSW-FSET
Faults with a WSW-ENE orietation below the Zechstein Group within the G&L Platform
G en L Platform sub-salt WSW-ENE Fault Set
GLP-SUB-WSW-ENE-FSET
Faults with a WNW-ESE orietation below the Zechstein Group within the G&L Platform
G en L Platform sub-salt WNW-ESE Fault Set
GLP-SUB-WNW-ESE-FSET
Faults with a N-S W orietation below the Zechstein Group within the G&L Platform
G en L Platform sub-salt NNW-SSE Fault Set
GLP-SUB-NNW-SSE-FSET
The Holsloot Fautl System transects the Lower Saxony Basin in its western part and divides a structurally deeper basin in the east from a shallower basin in the west. Plausibly the Holsloot Fault System forms the connection between the Western Lauwerzee Trough Fault System and the Gronau Fault System
Holsloot Fault System
NNW-SSE oriented fault zone active during the Paleozoic (Westphalian C and -D), also referred to as Osning-Gronau Fault System
Gronau Fault System
GR-FS
Undifferentiated faults within the Lauwerzee Through. The domain extents northward in the offshore where it merges with the Ameland Platform
Lauwerzee Trough Fault Domain
LZT-FD
The fault pattern above the salt is relatively simple and contains several long regional fault zones as well as smaller-scale faults associated with salt structures (diapirs and ridges). The salt structures, however, have a genetic and to some extent locational relationship to large offset faults below the salt (the sub-salt faults)
Lauwerzee Trough supra-salt Fault Domain
LZT-SUPRA-FD
A complex fault pattern at Rotliegend and deeper stratigraphic levels that cannot be easily related to one single phase of faulting with one single stress orientation. More likely, the faults and fault zones evolved through multiple phases of fault activity. Early Carboniferous carbonate platforms are generally bounded by NW-SE faults supporing the notion that these are long-lived Paleozoic structures. The lack of similarly faulted Rotliegend outcrop analogues and the fact that these strain features can thus only be studied in seismic data leaves room for multiple interpretations
Lauwerzee Trough sub-salt Fault Domain
LZT-SUB-FD
In origin the Hantum Fault System is a Variscan structure that separates the Friesland PLatform from the Terschelling Basin to the North. It was likely instrumental in defining the northern limit of the Lower Carboniferous carbonate platform on the Friesland Platform. The fault system extents to the northwest, probably across the Dutch Central Graben where it may form (or merges) with the Northern Cleaver Bank Margin Fault System. To the southeast it is thought to cross the Lauwerzee Trough where it becomes overprinten by multiple younger faults with various orientations
Hantum Fault System
H-FS
In the eastern part of the Netherlands, the Raalte Boundary Fault System is the southermost marginal fault of the Friesland Platform s.l.
Raalte Boundary Fault System
RB-FS
The Friesland Platform represents a large and geologically diverse area and is characterised by multiple fault orientations both below and above the Zechstein salt. Early Carbinferous carbonate platforms are generally bounded by NE-SE faults supporing the notion that these are long-lived Paleozoic structures. The platform experienced Middle to Late Jurassic erosion (Mid and Late Kimmerian unconformity). In the north -eastern and southern part of the Friesland Platform, the Triassic can reach a thickness up to 800 m. In the northeast, the Friesland Platform is fault-bounded by the Lauwerszee Trough. Towards the southwest, the Texel-IJsselmeer High forms the boundary. In the northwest, the Friesland Platform passes into the Late Jurassic - Early Cretaceous Vlieland Basin and in the southeast towards the Lower Saxony Basin.
Friesland Platform Fault Domain
FP-FD
A series of WNW-ESE trending step faults forming the northern margin of the Dalfsen High
Northern Dalfsen Faults Set
ND-FSET
The Dalfsen High (DH) is a relatively small isolated high on the Friesland Platform on strike with the Texel-IJsselmeer High, bounded to te south by the Raalt Boundary Fault System and transected by WNW-ESE fauts. It is characterised by Cretaceous sediments on top Carboniferous rocks. In the area surrounding the DH, the Triassic has been eroded, which points to a Jurassic or more recent phase of uplift. The northern margin is defined by the Northern Dalfsen Fault Set
Dalfsen High Fault Domain
DH-FD
En-echelon pattern of NNE-SSW trending faults forming the transition to the Dalfsen sub Domain
Eastern Friesland Platform Fault Domain
E-FP-FD
Undifferentiated faults above the Zechstein Group within the Friesland Platform
Friesland Platfrom supra-salt Fault Domain
FP-SUPRA-FD
Faults with a NNE-SSW orietation below the Zechstein Group within the Friesland Platform
Friesland Platform sub-salt NNE-SSW Fault Set
FP-SUB-NNE-SSW-FSET
Faults with a WSW-ENE orietation below the Zechstein Group within the Friesland Platform
Friesland Platform sub-salt WSW-ENE Fault Set
FP-SUB-WSW-ENE-FSET
Faults with a ESE-WNW orietation below the Zechstein Group within the Friesland Platform
Friesland Platform sub-salt WNW-ESE Fault Set
FP-SUB-WNW-ESE-FSET
Friesland Platform sub-salt NNW-SSE Fault Set
FP-SUB-NNW-SSE-FSET
In the Dutch territory, the Dowsing-South Hewett Large Scale Fault System marks a strong and long-lived contrast between the Wales-Brabant massif and Southern North Sea Basin that was repeatedly reactivated since at least the Carboniferous. The Dowsing-South Hewett Fault Zone, was active during the Carboniferous and possibly earlier times. However, The northwestward continuation as southern boundary of the Calledonian Southern North Sea Lüneberg Terrane is unclear as it does not cross the Southern Uplands/Mid North Sea high.
Dowsing-South Hewett Large Scale Fault System
DSH-LFS
Eastern part of the Dowsing-South Hewett Large Scale Fault System that defines the southern boundary of the West Netherland Basin - Ruhr Valley Graben Basin basin system
Southern West Netherlands Basin - Ruhr Valley Graben Fault System
S-WNB-RVG-FS
Aligned group of normal faults forming the southwestern border zone of the RVG that were active mainly during the Cenozoic extension but might originate from older faults
FeldBiss sub Fault System
FBS-sFS
Veldhoven sub Fault System
VEH-sFS
Group of normal faults in the southwestern border zone of the West Netherland Basin that were active during the Mesozoic and - to a lesser extent- Cenozoic extension and inversion phases . They might originate from older faults
Southern West Netherlands Basin sub Fault System
S-WNB-sFS
A fault system defined by 1) the South Hewett Fault zoney that forms the southern boundary of the Late Permian-Mesozoic Sole Pit trough and 2) its westward continuations into the Dowsing Fault zone that forms the southern margin faults zone of the the Late Permian-Mesozoic Silverpit basin in the UK sector
Dowsing-South Hewett Fault System
DSH-FS
This vocabulary describes a) the hierarchical classification of shear displacement structures and b) parameters used in the attribute list of the HIKE fault data base that extend existing INSPIRE and/or GeoSciML code lists
Klassifikation Tektonischer Grenzflächen
A formal classification scheme for the elements of the HIKE fault data base that allows a hierarchical ranking of mostly shear displacement structures like e.g. faults, shear zones. It is mainly base on Hintersberger et al. (2017), but has been extended to include further concepts from other countries.
Fault classification terms and parameters
Fault classification term
A formal classification scheme for the elements of the HIKE fault data base that allows a hierarchical ranking of mostly shear displacement structures like e.g. faults, shear zones and fissures. It is mainly base on Hintersberger et al. (2017), but has been extended to further concepts in order to describe the tectonic frame work of other countries.
Tectonic Boundary
Tektonische Grenzfläche
A Tectonic Boundary is a shear displacement structure separating tectonic units and includes all brittle to ductile style structures along which displacement has occurred, from a simple, single 'planar' brittle or ductile surface to a fault system comprised of tens of strands of both brittle and ductile nature (after GeoSciML Modeling Team, 2017).
Eine Tektonische Grenzfläche ist eine Scherfläche, die tektonische Einheiten trennt und alle spröden bis duktilen Strukturen einschließt, entlang denen die Verschiebung stattgefunden hat, von einer einfachen, einzelnen „planaren“ spröden oder duktilen Fläche bis zu einem Störungssystem bestehend aus mehreren spröden und/oder duktilen Anteilen (nach GeoSciML Modeling Team, 2017).
Step fault
Large-scale Fault System
In the hierarchical ranking, fault systems are merged into a Large-scale Fault System (LFS) if their extent and impact on the orogenic evolution are of transregional importance (i.e. the Periadraric-Mid-Hungarian Large-scale Fault system for the Alpine Orogen).
Großstörungssystem
A Large-scale Fault System (LFS) corresponds to the highest level of the Tectonic Boundaries Classification Scheme and describes an alignment of connected and kinematically related fault systems that extend transregionally, typically over hundreds of kilometers. (Hintersberger et al. 2017:197).
Ein Großstörungssystem entspricht der höchsten Stufe in der Klassifikation zu Tektonischen Grenzflächen und beschreibt eine Anordnung von verbundenen und kinematisch in Beziehung stehenden Störungssystemen, die sich überregional und typischerweise über Hunderte von Kilometern erstrecken (Hintersberger et al. 2017:197).
Fault System
Störungssystem
For example, the Salzach-Ennstal-Mariazell-Puchberg (SEMP) Fault System (Ratschbacher et al., 1991a, b; Decker et al., 1994; Linzer et al., 2002) is a 400 km long ENE–WSW trending fault system consisting of several faults.
A Fault System corresponds to an alignment of connected and kinematically related faults and/or shear zones active during at least one or potentially several geological events and that may contain different deformation styles (modified after Neuendorf et al., 2005). The faults within a fault system must be related spatially and kinematically at least during one main deformation event (Hintersberger et al., 2017:198).
Eine Anordnung von (miteinander) verbundenen und kinematisch in Beziehung stehenden Störungen und/oder Scherzonen, welche über einen längeren geologischen Zeitraum (mehrere Perioden/Stufen/Events) aktiv sind und mehrere Deformationsarten beinhalten können (verändert nach Neuendorf et al., 2005). Die Störungen innerhalb eines Störungssystems müssen räumlich und kinematisch, zumindest während eines Haupt-Deformationsereignisses, mitneinander in Beziehung stehen (Hintersberger et al., 2017:198).
Fault
In the German the terms 'Verwerfung', 'Verwurf', 'Bruch' and 'Abbruch' are used as synonyms for faults. The terms 'Bruch' and 'Abbruch' are associated with normal faulting kinematics.
Störung
The term fault is used here in the sense of a discrete deforming interface separating two rock masses along which one mass has slid past the other (Neuendorf et al., 2005). Deformation in faults is dominated by brittle deformation mechanisms (Schultz & Fossen, 2008). (Hintersberger et al., 2017:198)
Eine diskrete tektonische Grenzfläche oder Zone diskreter Flächen, welche zwei Gesteinskörper/massen trennt und an derer parallel Bewegung stattgefunden hat (Neudendorf et al., 2005). Im allgemeinen Verständnis dominieren spröde Deformationsmechanismen (Schultz & Fossen, 2008). (Hintersberger et al., 2017:198)
Verwurf
Bruch
Abbruch
Verwerfung
Subfault
Teilstörung
A subfault is a subordinated discrete interface separating two rock masses along which one mass has slid past the other, belonging to an ordinated fault (Neuendorf et al., 2005). (Hintersberger et al., 2017:199)
Eine Teilstörung ist, eine der Störung untergeordnete, diskrete Grenzfläche, die zwei Gesteinsmassen trennt und an der Bewegung stattgefunden hat (Neuendorf et al., 2005). (Hintersberger et al., 2017:199)
Shear zone
Shear zones may contain either brittle or ductile fault rocks. Here, deformation in shear zones is dominated by ductile deformation mechanisms (Schultz & Fossen, 2008, and references therein) involving dynamic recrystallization, diffusive mass transfer, dislocation creep and/or grain-boundary sliding. It also includes the term “Mylonite Zone” describing relatively thick zones of intensive ductile shearing (Mawer, 1986).
Scherzone
A broad planar zone of relatively intense localised deformation (shearing) in which progressive deformation is non-coaxial (Passchier & Trouw, 1996; Hintersberger et al., 2017:198).
Breite planare Zone lokalisierter und relativ intensiver Deformation, in der die progressive Deformation nicht-koaxial (scherend) ist (Passchier & Trouw, 1996; Hintersberger et al., 2017:198).
Subfault System
Shear displacement structures containing at least a ductile and a brittle part are hierarchically considered as a Subfault System. For example, the Brenner SFS consists of the ductile lowangle Brenner Shear Zone and the steeper brittle Brenner Fault.
Teilstörungssystem
A Subfault System is a part of a fault system defined by spatial, temporal or kinematic characteristics that are different from the overall deformation of the related fault system during at least one main deformation event (Hintersberger et al., 2017:198).
Teil eines Störungssystems, welcher sich aus Störungen und/oder Scherzonen zusammensetzt und einen räumlich, zeitlich, beziehungsweise kinematisch in Beziehung stehenden Teilabschnitt definiert, welcher sich durch mindestens einen Hauptdeformations-Event vom zugehörigen Störungssystem unterscheiden lässt (Hintersberger et al. 2017:198).
Störungszone
Fault Zone
Volcanic system
Fissure Set
Fissure
Fissures are volcanic vents. They present as linear features on the surface and are created by the non-explosive eruption of lava. In some cases the fissures make rows of craters.
Fault Set
The category 'Fault Set' is mostly used for (sub-)parallel oriented faults in orogens, e.g. the Northern Calcareous Alps, which are subdivided into five groups striking NNE–SSW, NE–SW, ENE–WSW, E–W, NW–SE, respectively.
Störungsset
A Fault Set describes an alignment of parallel trending faults that are kinematically and temporally linked, but where the spacing between the single fault zones exceeds the displacement observed along the fault. It does not correspond to the term “fault zone” (Hintersberger et al., 2017:198).
Der Begriff Störungsset definiert eine Anordnung von parallel verlaufenden (Teil-)Störungen, welche kinematisch und zeitlich in Verbindung stehen, wobei aber die Abstände zwischen den einzelnen Störungen (im Gegensatz zu Störungszonen) den beobachteten Versatz entlang der Störungen übertrifft (Hintersberger et al., 2017:198).
Nappe Boundary
The term describes a discrete, brittle or ductile, shearing horizon between tectonic units (e.g. nappes, nappe systems). In this definition, „discrete“ refers to map scale, since in the field a nappe boundary can correspond to a diffuse tectonic mélange zone with elements of both units that it separates (Hintersberger et al. 2017:199).
Base of Nappe
Fault Domain
In contrast to Large-scale Fault Systems (LFS) which are more or less linear alignment of (sub-)parallel faults or fault systems, the term 'Fault Domain' applies for areal (non-linear) terrains of similar fault pattern. If any confusion with geological domains would arise, the term 'fault realm' could be used for clarification purposes.
Domäne
Fault domain describes an area/terrain of similar pattern of fault array implying a similar tectonic regime. Direct subsets can be Subdomains, Fault Systems and/or Faults
Domäne bezeichnet ein Gebiet mit ähnlichen Störungsmustern, die ein vergleichbares tektonisches Regime implizieren. Untereinheiten können Subdomänen, Störungssysteme und/oder Störungen sein.
Fault Realm
structural domain
Fault Subdomain
Fault Subdomain is a subset of Fault domain. This category can be used to distinguish between areas of (subordinate) differenes of fault pattern within a Fault domain. If linear arrays of faults are distinguished the term 'Fault System' applies.
Subdomäne
Fault subdomains describes distinguishable areas of closely similar pattern of fault array within a Fault domain.
Subdomänen bezeichen unterscheidbare Gebiete sehr ähnlicher Störungsmuster innerhalb einer Domäne.
Fault Swarm
A fault swarm is an array of discrete faults with small offsets of same type and formed during the same deformation episode, most probably resulting from distortion caused by movment of blocks along faults with curved profiles (Laubach et al., 1992, 1995).
Fault Cluster
Störungsschwarm
A Fault Swarm is not necessarily linearly arranged, whereas the fault chain describes a linear array of faults.
Fault Chain
Störungszug
A string (linear array) of faults (including minor subfaults) inferred to represent one single supraregional fault. Faults of the same type and formed during the same deformation episode.
Fault Train
Attribute parameters of the HIKE fault data base
Here, parameters describing the fault attributes of the HIKE European Fault Database are listet. In general, attribute parameters were choosen to be as close as possible in accordance with INSPIRE and GeoSciML codelists, but mostly do not exactly match the description nor its purpose in the INSPIRE or GeoSciML data model. Additional fault attribute parameters that do not appear in the INSPIRE registry are defined in this Project Vocabulary.
Maximum displacement
Displacement in meters as measurement in map view. The default displacement is measured perpendicular to the fault line/trace. If the sense of movement is either (normal/reverse_)dextral or (normal/reverse_)sinistral, the displacement is measured parallel to the fault trace.
Fault type
The fault type is defined exactly as proposed in the INSPIRE registry. Additional fault types that do not appear in the INSPIRE registry are defined in this Project Vocabulary
fault (INSPIRE)
A discrete surface, or zone of discrete surfaces, with some thickness, separating two rock masses across which one mass has slid past the other.
INSPIRE codelists
high angle fault
Fault that dips at least 45 degrees over more than half of its recognized extent, for which slip or separation is not explicitly specified.
low angle fault
Fault that dips less than 45 degrees over more than half of the recognized extent of the fault.
ring fault
caldera fault
A ring fault, also known as caldera fault, is a fault that occur within a collapsed volcanic caldera and the site of bolide strikes, such as the Chesapeake Bay impact crater. Ring faults are result of a series of overlapping normal faults, forming a circular outline.
Related subsurface activity
Known human subsurface activities in relation to the fault. The definition of the attribute parameters is related to the INSPIRE code list BoreholePurposeValue, but do not exactly match the description.
Exploration of groundwater
Activity for examination of the subsurface with regard to the extraction of groundwater from an aquifer for various purposes (domestic, industrial, water supply intake and other)
Entnahme von Grundwasser aus einem Grundwasserleiter zu verschiedenen Zwecken (Haushalte, Industrie, Wasserversorgung und andere)
Exploration of minerals
Activity for examination of the subsurface with regard to the locating and/or extracting mineral resources from the subsurface.
Exploration of geothermal energy
Activity for examination of the subsurface with regard to the utilization of geothermal energy resources and design of geothermal heat pumps.
Exploration of oil & gas
Activity for examination of the subsurface with regard to the availability of fossil energy resources and planning the extraction thereof.
Offset determination
Method how the displacement at a fault has been determined.
Fault offset determination
well/seismic interpretation
This term refers to the determination of displacement across a (mostly buried) fault based on interpretation of well and/or seismic information
crosscutting relationships
This term refers to the principle of cross-cutting relationships for the determination of displacement across a fault. Cross-cutting relationships is a principle of geology that states that the geologic feature which cuts another is the younger of the two features. It is a relative dating technique in geology.
displacement on maps
This term refers to the determination of displacement across a fault based on information shown on geological maps
paleoseismicity
This term Paleoseismicity refers to geologically recorded earthquakes, most of them unknown from human descriptions or seismograms. Geologic records of past earthquakes can include faulted layers of sediment and rock, injections of liquefied sand, landslides, abruptly raised or lowered shorelines, and tsunami deposits
palaeogeography
This term describes the usage of paleogeographic reconstructions for the determination of the amount of displacement across a fault.
sediment structures
This term refers to the determination of displacement across a fault based on sediment structures
seismicity
This term refers to the determination of displacement across a fault based on seismological information shown on geological maps
field observation
This term refers to the determination of displacement across a fault based on geological field observations such as shear sense indicators or offset observed at outcrop scale.
microfabrics
This term refers to the usage of microfabric analysis to determine the characteristics of displacement across a fault. The microstructural characterization of a crystalline material includes the determination of grain number and size distribution, chemical composition, spatial distribution of phases, crystallographic and structural relationships between grains as well as intragranular misorientation.
paleostress measurements
This term refers to the determination of displacement across a fault based on paleostress analyses.
Evaluation method
The information given for the “evaluation method” is used as a rough quality measure for the following fault attribute set. It should give a qualitative statement how reliable the observations and the derived fault attributes are. The definition of the attribute parameters is partly related to the GeoSciML classifier code list MappedFeatureObservationMethod , but do not exactly match the description and does not include all options.
direct observation
This evaluation method describes the highest evaluation quality, which related to a "direct visual observation", e.g. at an outcrop at the surface.
observed at depth
this evaluation method describes the fact that the respective tectonic boundary has been observed at depth and the fault is generelly assumed to be buried.
inferred
The evaluation method “inferred” describes that the fault is neither directly observed at the surface nor observed at depth by reliable methods, but its location and specification are based on inference from available evidence.
Movement sense
Movement sense describes the relative direction of movement of bodies of rock across a fault surface, as defined by the IUGS Commission for Geoscience Information (CGI) Geoscience Terminology Working Group.
normal sinistral
detachment
dextral
sinistral
reverse sinistral
thrust
generic decollement
normal dextral
reverse
no movement sense
normal
reverse dextral
thrust decollement
Strike
trend
For the purpose of the HIKE fault database, the faults are sorted into strike categories. Directions are classified in 8 classes of each 22,5 degrees (WNW-ESE, NW-SE, NNW-SSE, N-S, NNE-SSW, NE-SW, ENE-WSW, E-W).
Strike is defined as the compass direction, relative to north, of the line formed by the intersection of a rock layer or other planar feature with an imaginary horizontal plane. The intersection of two flat planes is a straight line, and in this instance, the line is geologic strike.
Dip direction
For the purpose of the HIKE European fault database, the faults are sorted into dip direction categories. Directions are classified in 16 classes of each 22,5 degrees (N, NNE, NE, ENE, E, ESE, SE, SSE, S, SSW, SW, WSW, W, WNW, NW, NNW).
Dip direction is the azimuth perpendicular to the strike of the structure.
Observation method
Observation method gives an overview of the most important methods how the location and the characteristics of a fault objects were obtained. The list of possible methods is based on the INSPIRE codelist entries of “SurveyTypeValue” and includes some definitions of the GeoSciML vocabulary entry “MappedFeature ObservationMethod”, but do not exactly match the description nor its purpose in the INSPIRE or GeoSciML data model.
airborne Geophysical Survey
The fault and its characteristics have been observed during a campaign of airborne geophysical measurements, where the geophysical data is obtained by an apparatus fixed to a helicopter, fixed wing, or ultra light aircraft, depending on location and topographic relief.
seismological Survey
The fault and its characteristics have been observed during a campaign of seismological measurements, where vibrations from natural earthquakes or rupture processes (due to hydraulic stimulation) are used as a source for structural imaging of the subsurface.
2D Seismic Survey
The fault and its characteristics have been observed during a campaign of 2D seismic measurements, where the behavior of artificially-generated seismic waves in the subsurface is recorded. A seismic wave or pulse is generated at the surface by an active seismic source which can be a vibration, mechanical impact, or near-surface explosion.
observed borehole material
The fault and its characteristics have been directly observed in material obtained from a borehole (e.g., borehole core). If the observation method is “observed borehole material”, the evaluation method (see section 4.4.1.1) should be given as “direct observation”.
magnetotelluric Survey
The fault and its characteristics have been observed during a campaign of magnetotelluric measurements where the electrical resistivity structure of the subsurface is measured through the measurement of electrical and magnetic fields at the earth's surface.
2D Resistivity Survey
The fault and its characteristics have been observed during a campaign of 2D multi-electrode direct current measurements, in which current is applied to the ground using electrodes and the earth response (voltage or potential difference) is recorded and presented as a 2D geoelectric section showing apparent resistivity distribution.
time-domain EM Survey
The fault and its characteristics have been observed during a campaign of The option “observed at depth” refers to the fact that the respective fault information has been observed at depth and the fault is generally assumed to be buried.
inferred projection between observed locations
The determination of the location of the fault, its existence or/and its characteristics is based on inferred continuity with observed locations, and assumption of continuity of the feature. If “inferred projection between observed locations” is given, the evaluation method (see section 4.4.1.1) should be set as “inferred”.
3D Seismic Survey
The fault and its characteristics have been observed during a campaign of 3D seismic measurements, where the behavior of artificially-generated seismic waves in the subsurface is recorded. A seismic wave or pulse is generated at the surface by an active seismic source which can be a vibration, mechanical impact, or near-surface explosion.
sonar Survey
The fault and its characteristics have been observed during a campaign of sonar (sound navigation and ranging) measurements, where underwater sound propagation is used, among other applications, for bathymetric mapping, sub-bottom profiling, and gas leak detection.
observed outcrop
The fault and its characteristics have been observed and located directly in outcrop(s), where geologist(s) occupied location of phenomenon, and traced it explicitly over mapped extent. If the observation method is “observed at outcrop”, the evaluation method (see section 4.4.1.1) should be given as “direct observation”.
3D Resistivity Survey
The fault and its characteristics have been observed during a campaign of 3D multi-electrode direct current measurements, in which current is applied to the ground using electrodes and the earth response (voltage or potential difference) is recorded and presented as a 3D block showing apparent resistivity distribution.
georadar survey
The fault and its characteristics have been observed during a campaign of ground penetrating radar (GPR) or georadar, where high-frequency electromagnetic waves are used to map below-ground lithology or buried objects.
frequency Domain EM Survey
The fault and its characteristics have been observed during a campaign of frequency-domain electromagnetic (EM) measurements, where the electrical conductivity of the subsurface through electromagnetic induction is mapped by using continuous wave field methods.
ground Magnetic Survey
The fault and its characteristics have been observed during a campaign of surface magnetic measurements, recorded at an observation point on the earth's surface.
1D Resistivity Survey
The fault and its characteristics have been observed during a campaign of vertical electric sounding measurements, which provides information regarding the change in apparent resistivity of the subsurface with depth.
ground Gravity Survey
The fault and its characteristics have been observed during a campaign of surface gravity measurements, recorded at an observation point on the earth's surface.
VSP Survey
The fault and its characteristics have been observed during a campaign of Vertical Seismic Profiling (VSP), where the detectors for seismic measurements are in a borehole.
CPT Survey
The fault and its characteristics have been observed during a campaign of cone penetration test (CPT) sounding measurements, where the geotechnical engineering properties of soils are determined by pushing an instrumented cone into the ground at a controlled rate.
borehole Logging Survey
The fault and its characteristics have been observed during a campaign of borehole logging, where physical, chemical, and structural properties of penetrated geological formations are measured using tools that are lowered into a borehole on a wireline cables.