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Africa
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Western U.S. (5)
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hydrogen
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stable isotopes
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C-13/C-12 (9)
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O-18/O-16 (7)
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Pb-208/Pb-204 (1)
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S-34/S-32 (3)
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metals
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U-238/Pb-206 (1)
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iron
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Fe-56/Fe-54 (1)
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lead
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Pb-206/Pb-204 (1)
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platinum group
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rare earths
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nitrogen (1)
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oxygen
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O-18/O-16 (7)
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silicon
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sulfur
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S-34/S-32 (3)
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fossils
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Invertebrata
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Echinodermata
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Protista
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Vermes
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Plantae
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Pteridophyta
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geochronology methods
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Ar/Ar (4)
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geologic age
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Quaternary
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Siwalik System (1)
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Tertiary
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Asmari Formation (1)
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lower Tertiary (2)
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Neogene
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Etchegoin Formation (1)
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Miocene
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Antelope Shale (1)
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Burdigalian (2)
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middle Miocene
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Saddle Mountains Basalt (1)
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Temblor Formation (1)
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upper Miocene
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Messinian (3)
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Wanapum Basalt (1)
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Pliocene (9)
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Ringold Formation (1)
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upper Neogene (1)
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Paleogene
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Eocene
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Annot Sandstone (2)
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Crescent Formation (1)
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lower Eocene
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Wasatchian (1)
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Ypresian (1)
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middle Eocene (1)
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Swauk Formation (2)
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upper Eocene (1)
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Hanna Formation (1)
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Oligocene
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lower Oligocene (2)
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Paleocene
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lower Paleocene (1)
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Paleocene-Eocene Thermal Maximum (1)
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Wasatch Formation (1)
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Shahejie Formation (1)
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Tulare Formation (2)
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upper Cenozoic (1)
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Coal Measures (1)
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Dalradian (2)
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Lake Bonneville (1)
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Mesozoic
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Cretaceous
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Comanchean
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Buda Limestone (1)
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Paluxy Formation (1)
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Rodessa Formation (1)
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Lower Cretaceous
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Albian (1)
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Christopher Formation (1)
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Gething Formation (1)
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Hauterivian (1)
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Paluxy Formation (1)
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Pasayten Group (1)
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Rodessa Formation (1)
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Middle Cretaceous (1)
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Upper Cretaceous
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Buda Limestone (1)
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Duwi Formation (1)
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Gulfian
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Austin Chalk (1)
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Woodbine Formation (1)
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La Luna Formation (1)
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Maestrichtian (3)
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Neuquen Group (1)
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Santonian (2)
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Senonian (1)
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Franciscan Complex (1)
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Jurassic
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Lower Jurassic (3)
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Bowser Lake Group (1)
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lower Mesozoic (1)
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Navajo Sandstone (1)
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Passaic Formation (1)
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Triassic
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Lower Triassic
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Thaynes Formation (1)
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Sherwood Sandstone (1)
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Upper Triassic
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Keuper (1)
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Rhaetian
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upper Mesozoic (3)
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Yanshanian (3)
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Moldanubian (1)
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Paleozoic
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Arbuckle Group (1)
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Cambrian
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Acadian (1)
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Lancara Formation (2)
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Flathead Sandstone (1)
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Mount Read Volcanics (1)
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Tintic Quartzite (1)
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Carboniferous
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Benxi Formation (1)
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Lower Carboniferous
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Dinantian (1)
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Mississippian
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Macumber Formation (1)
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Middle Mississippian
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Visean (1)
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Upper Mississippian
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Mauch Chunk Formation (1)
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Meramecian (1)
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Windsor Group (1)
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Pennsylvanian
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Cumberland Group (2)
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Joggins Formation (1)
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Middle Pennsylvanian
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Paradox Formation (1)
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Minturn Formation (1)
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Pottsville Group (1)
-
-
Upper Carboniferous (2)
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Catskill Formation (1)
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Devonian
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Gile Mountain Formation (1)
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Guilmette Formation (1)
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Lower Devonian
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Oriskany Sandstone (1)
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Middle Devonian
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Eifelian (1)
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Givetian (2)
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Hamilton Group (1)
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Mahantango Formation (2)
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Marcellus Shale (1)
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Prairie Evaporite (1)
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Tully Limestone (1)
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Old Red Sandstone (1)
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Upper Devonian
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Brallier Shale (1)
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Frasnian (1)
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-
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Exshaw Formation (1)
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Helderberg Group (1)
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lower Paleozoic (2)
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Ordovician
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Ely Springs Dolomite (1)
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Lower Ordovician
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Tremadocian
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Halifax Formation (1)
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Martinsburg Formation (1)
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Middle Ordovician
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Decorah Shale (1)
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Galena Dolomite (1)
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Platteville Formation (1)
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Saint Peter Sandstone (1)
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Upper Ordovician
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Caradocian (1)
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Maquoketa Formation (1)
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Wufeng Formation (1)
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Utica Shale (1)
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Permian
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Lower Permian
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Al Khlata Formation (1)
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Upper Permian (2)
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Silurian
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Lower Silurian (3)
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Salina Group (1)
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Taiyuan Formation (2)
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Tensleep Sandstone (1)
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upper Paleozoic
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Pictou Group (1)
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Shanxi Formation (2)
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Tirrawarra Sandstone (1)
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Waits River Formation (2)
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Wells Formation (1)
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Precambrian
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Archean
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Bulawayan Group (1)
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Iron Ore Group (1)
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Mesoarchean (2)
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Neoarchean
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Singhbhum Granite (1)
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Swaziland Supergroup (1)
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Yellowknife Group (1)
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Biwabik Iron Formation (1)
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Missi Group (1)
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Stirling Quartzite (1)
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upper Precambrian
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Proterozoic
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Algonkian
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Baraboo Quartzite (1)
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Huronian (2)
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Hutuo Group (1)
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Neoproterozoic
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Moinian (2)
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Ortega Group (1)
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Paleoproterozoic
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Aphebian
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Hurwitz Group (1)
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-
-
-
-
Vadito Group (1)
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Ventersdorp Supergroup (1)
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Witwatersrand Supergroup (1)
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-
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igneous rocks
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igneous rocks
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carbonatites (1)
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plutonic rocks
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diabase (1)
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gabbros
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granites
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charnockite (3)
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granodiorites (3)
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ultramafics
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volcanic rocks
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andesites (2)
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basalts
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flood basalts (2)
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pyroclastics
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hyaloclastite (1)
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tuff (5)
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rhyolites (2)
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ophiolite (2)
-
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metamorphic rocks
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metamorphic rocks
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amphibolites (2)
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gneisses
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orthogneiss (1)
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marbles (2)
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metaigneous rocks
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metasedimentary rocks
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metasomatic rocks
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skarn (3)
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metavolcanic rocks (3)
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migmatites (2)
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mylonites
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phyllites (3)
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quartzites (8)
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schists
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greenstone (1)
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slates (4)
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ophiolite (2)
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turbidite (7)
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minerals
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carbonates
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calcite (2)
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dolomite (2)
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native elements
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graphite (2)
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oxides
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hydroxides
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iron oxides (1)
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phosphates
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apatite (3)
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silicates
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framework silicates
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feldspar group
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alkali feldspar
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K-feldspar (1)
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silica minerals
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jasper (1)
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orthosilicates
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zircon (5)
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sheet silicates
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mica group
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sulfates
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anhydrite (2)
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barite (1)
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sulfides
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molybdenite (1)
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stibnite (1)
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Primary terms
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absolute age (12)
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Africa
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East Africa
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Ethiopia (1)
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North Africa
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Egypt
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Morocco
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Southern Africa
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Namibia
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South Africa
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Arctic Ocean
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Arctic region
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Asia
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Altai Mountains
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Altai Russian Federation
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Far East
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China
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Indonesia
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Mongolia (1)
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Himalayas
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Indian Peninsula
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Gujarat India
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Karnataka India
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Chitradurga schist belt (1)
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Kolar Gold Fields India (1)
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Narmada-Son Lineament (1)
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Jammu and Kashmir
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Kashmir (1)
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Nepal (1)
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Pakistan
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Punjab Pakistan
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Salt Range (1)
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Potwar Plateau (2)
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Irkutsk Russian Federation (1)
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Main Boundary Fault (2)
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Middle East
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Iran (8)
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Zagros (7)
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Sayan
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Siberian fold belt (1)
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Atlantic Ocean
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South Atlantic
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Australasia
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Australia
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Western Australia
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Capricorn Orogen (1)
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Papua New Guinea (1)
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bauxite deposits (1)
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Canada
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Meguma Terrane (1)
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Newfoundland and Labrador
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Ontario
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Cochrane District Ontario
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Quebec
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Matapedia County Quebec (1)
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Northumberland Strait (1)
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Nunavut
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Axel Heiberg Island (3)
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Queen Elizabeth Islands
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Axel Heiberg Island (3)
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Western Canada
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Alberta
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British Columbia
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Northwest Territories
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Yellowknife Northwest Territories (1)
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Saskatchewan (1)
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Yukon Territory (1)
-
-
-
carbon
-
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GeoRef Categories
Era and Period
Epoch and Age
Book Series
Date
Availability
synclines
Structural inheritance controls crustal-scale extensional fault-related folding in the Exmouth and Dampier Sub-basins, North West Shelf, Australia Available to Purchase
Configuration of Carbonatite Constrained in Preintrusion Transpositional Foliation in the Bayan Obo Giant Rare Earth Element Deposit, China Available to Purchase
New details on the volcanic and tectonic evolution of the Mesoarchaean Dominion Group with special reference to the Syferfontein Formation in the Ottosdal area (South Africa) Available to Purchase
Formation of a dome-and-basin fold interference pattern by granite intrusions Available to Purchase
New Seismic Imaging of the Crustal Structure beneath the Eastern Sichuan and Wuling Mountains, South China: Insights into the Formation of Fold‐and‐Thrust Belts Available to Purchase
Petrological and Geochemical Characterization of Miocene Tipam Sandstone in Parts of Cachar Fold Belt, Northeast India Available to Purchase
High‐Resolution Shear‐Wave Velocity Structure of the 2019 M s 6.0 Changning Earthquake Region and Its Implication for Induced Seismicity Available to Purchase
Analogue modeling of domino-style extensional basement fault systems with prekinematic salt Available to Purchase
Oligocene–late Miocene basin evolution in the Yengejeh syncline in the Central Iranian Basin in response to the Arabia–Eurasia orogeny Available to Purchase
Quantitative analysis of fault-and-fold growth in a transtensional basin: the Sørvestsnaget Basin, Western Barents Sea Available to Purchase
Abstract The growth of faults and folds in basins formed under transtension has been less studied than that in their extensional counterparts. In this study, we capitalize on 3D seismic reflection data to investigate the evolution of faults and folds that evolved coevally during suborthogonal partitioned extension and shortening, respectively, in the Sørvestsnaget Basin, Western Barents Sea. We use quantitative techniques to constrain the distribution of normal fault throw, shortening accommodated by folds and thrusts, and stratigraphic thickness variations, to analyse the relative temporal and spatial evolution of faults and folds. Our results show that normal faults display a similar evolution to those occurring in extensional basins, where they grew by lateral- and dip-linkage of individual fault segments as well as upward propagation. Notably, we show that shortening-related fold growth affected the fault growth patterns, skewing their throw distributions, and shifting the location of accommodation away from the evolving folds. Thus, fold amplification caused lateral migration of normal fault hanging-wall depocentres. Our results shed new light on fault-and-fold growth processes in transtensional basins and contribute to an improved understanding of the structural evolution of basins forming along sheared continental margins, which has economic implications for sheared-margin basins targeted for hydrocarbon exploration.
Evolution of rift-related cover-basement decoupling revealed by brecciation processes in the eastern Pyrenees Open Access
Complicated Fault Characterization and Its Influence on Shale Gas Preservation in the Southern Margin of the Sichuan Basin, China Open Access
Evidence for large departures from lithostatic pressure during Late Cretaceous metamorphism in the northern Snake Range metamorphic core complex, Nevada Available to Purchase
ABSTRACT The highest-grade Barrovian-type metamorphic rocks of the North American Cordillera exposed today are Late Cretaceous in age and found within an orogen-parallel belt of metamorphic core complexes for which the tectonic histories remain controversial. Thermobarometric studies indicate that many of these Late Cretaceous metamorphic assemblages formed at pressures of >8 kbar, conventionally interpreted as >30 km depth by assuming lithostatic conditions. However, in the northern Basin and Range Province, detailed structural reconstructions and a growing body of contradictory geologic data in and around the metamorphic core complexes indicate these metamorphic rocks are unlikely to have ever been buried any deeper than ~15 km depth (~4 kbar, lithostatic). Recent models controversially interpret this discrepancy as the result of “tectonic overpressure,” whereby the high-grade mineral assemblages were formed under superlithostatic conditions without significant tectonic burial. We performed several detailed studies within the Snake Range metamorphic core complex to test the possibility that cryptic structures responsible for additional burial and exhumation might exist, which would refute such a model. Instead, our data highlight the continued discordance between paleodepth and paleopressure and suggest the latter may have reached nearly twice the lithostatic pressure in the Late Cretaceous. First, new detrital zircon U-Pb geochronology combined with finite-strain estimates show that prestrain thicknesses of the lower-plate units that host the high-pressure mineral assemblages correspond closely to the thicknesses of equivalent-age units in adjacent ranges rather than to those of the inferred, structurally overridden (para) autochthon, inconsistent with cross sections and interpretations that assume a lower plate with a deeper origin for these rocks. Second, new Raman spectroscopy of carbonaceous material of upper- and lower-plate units identified an ~200 °C difference in peak metamorphic temperatures across the northern Snake Range detachment but did not identify any intraplate discontinuities, thereby limiting the amount of structural excision to motion on the northern Snake Range detachment itself, and locally, to no more than 7–11 km. Third, mapped geology and field relationships indicate that a pre-Cenozoic fold truncated by the northern Snake Range detachment could have produced ~3–9 km of structural overburden above Precambrian units, on the order of that potentially excised by the northern Snake Range detachment but still far short of expected overburden based on lithostatic assumptions. Fourth, finite-strain measurements indicate a shortening (constrictional) strain regime favorable to superlithostatic conditions. Together, these observations suggest that pressures during peak metamorphism may have locally reached ~150%–200% lithostatic pressure. Such departures from lithostatic conditions are expected to have been most pronounced above regions of high heat flow and partial melting, and/or at the base of regional thrust-bounded allochthons, as is characteristic of the spatial distribution of Cordilleran metamorphic core complexes during the Late Cretaceous Sevier orogeny.