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all geography including DSDP/ODP Sites and Legs
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Africa
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Shuaiba Formation (4)
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-
Barremian (2)
-
Berriasian (2)
-
Cupido Formation (1)
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Edwards Formation (6)
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Fredericksburg Group (1)
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Glen Rose Formation (3)
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Hauterivian (1)
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Hosston Formation (1)
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McMurray Formation (1)
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Mural Limestone (2)
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Neocomian (1)
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Pearsall Formation (1)
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Sligo Formation (4)
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Thamama Group (2)
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Valanginian (2)
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Zubair Formation (1)
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Middle Cretaceous (8)
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Upper Cretaceous
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Campanian (3)
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Coniacian (1)
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Eutaw Formation (1)
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Gulfian
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Austin Chalk (2)
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Austin Group (1)
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Eagle Ford Formation (1)
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K-T boundary (1)
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Maestrichtian (3)
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Rosario Formation (1)
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Santonian (2)
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Senonian (11)
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Turonian (4)
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Viking Formation (1)
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Jurassic
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Lower Jurassic
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lower Liassic (2)
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middle Liassic (2)
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upper Liassic (1)
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Middle Jurassic
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Aalenian (1)
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Callovian (1)
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Norphlet Formation (1)
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Upper Jurassic
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Arab Formation (1)
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Argovian (1)
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Cotton Valley Group (3)
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Haynesville Formation (1)
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Kimmeridgian (5)
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Oxfordian (8)
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Sequanian (2)
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Smackover Formation (6)
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-
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lower Mesozoic (1)
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Triassic
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Liard Formation (1)
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Lower Triassic
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Smithian (1)
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Middle Triassic
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Anisian (2)
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Doig Formation (1)
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Montney Formation (1)
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Takla Group (1)
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Upper Triassic
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Norian (1)
-
-
-
upper Mesozoic (1)
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MIS 11 (1)
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MIS 7 (2)
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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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Bonanza King Formation (1)
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Lower Cambrian
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Poleta Formation (2)
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Rome Formation (1)
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Shady Dolomite (3)
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Tommotian (1)
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Middle Cambrian (5)
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Upper Cambrian
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Bonneterre Formation (1)
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Maynardville Limestone (1)
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Wilberns Formation (1)
-
-
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Carboniferous
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Amsden Formation (1)
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Lower Carboniferous
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Dinantian (7)
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Middle Carboniferous (1)
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Mississippian
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Charles Formation (2)
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Lower Mississippian
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Chappel Limestone (1)
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Tournaisian (1)
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Middle Mississippian
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Visean (3)
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Mission Canyon Limestone (2)
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Upper Mississippian
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Chesterian (1)
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Meramecian
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Saint Louis Limestone (1)
-
-
-
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Pennsylvanian
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Excello Shale (1)
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Lower Pennsylvanian
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Morrowan (1)
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Marble Falls Group (1)
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Middle Pennsylvanian
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Atokan (2)
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Desmoinesian (2)
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Paradox Formation (1)
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Morrow Formation (1)
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Red Fork Sandstone (1)
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Strawn Series (3)
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Upper Pennsylvanian
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Canyon Group (1)
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Holder Formation (1)
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Missourian (2)
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Virgilian (1)
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-
-
Springer Formation (1)
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Upper Carboniferous
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Westphalian (1)
-
-
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Devonian
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Beaverhill Lake Group (5)
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Keg River Formation (11)
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Lower Devonian
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Coeymans Formation (2)
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Emsian (4)
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Manlius Formation (1)
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Pragian (1)
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Middle Devonian
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Detroit River Group (1)
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Dundee Limestone (1)
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Eifelian (4)
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Elk Point Group (3)
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Givetian
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Horn Plateau Formation (1)
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-
Jeffersonville Limestone (2)
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Onondaga Limestone (6)
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Prairie Evaporite (5)
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Winnipegosis Formation (5)
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Miette Complex (5)
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Ramparts Formation (1)
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Slave Point Formation (1)
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Swan Hills Formation (12)
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Upper Devonian
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Birdbear Formation (1)
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Duperow Formation (1)
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Famennian
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Wabamun Group (2)
-
-
Frasnian
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Leduc Formation (19)
-
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Grosmont Formation (2)
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Jefferson Group (1)
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Nisku Formation (10)
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Strunian (1)
-
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Waterways Formation (3)
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Ellis Bay Formation (1)
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Exshaw Formation (1)
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Helderberg Group (2)
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Keyser Limestone (1)
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Knox Group (1)
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Laborcita Formation (1)
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Lisburne Group (1)
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lower Paleozoic
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Conococheague Formation (1)
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Matapedia Group (2)
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Ordovician
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Chickamauga Group (1)
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Lower Ordovician
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Beekmantown Group (1)
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Ellenburger Group (1)
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Fillmore Formation (1)
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Prairie du Chien Group (2)
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Middle Ordovician
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Black River Group (2)
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Chazy Group (1)
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Chazyan (2)
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Table Head Group (1)
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Trenton Group (2)
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Upper Ordovician
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Ashgillian (2)
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Cincinnatian
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Richmondian (1)
-
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Katian (1)
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Sandbian (1)
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Trentonian (2)
-
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Permian
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Ecca Group (1)
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Guadalupian
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Bell Canyon Formation (1)
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Brushy Canyon Formation (2)
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Capitan Formation (14)
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Cherry Canyon Formation (1)
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Delaware Mountain Group (1)
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Grayburg Formation (3)
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Queen Formation (3)
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Seven Rivers Formation (2)
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Tansill Formation (5)
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Lower Permian
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Cherry Canyon Formation (1)
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Leonardian (3)
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Wolfcampian (3)
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Maokou Formation (5)
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Middle Permian (2)
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Upper Permian
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Changxing Formation (6)
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Yates Formation (3)
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Read Bay Formation (1)
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Silurian
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Lockport Formation (7)
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Lower Silurian
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Brassfield Formation (1)
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Llandovery (7)
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Wenlock (9)
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Middle Silurian
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Clinton Group (1)
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Guelph Formation (5)
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Keefer Sandstone (3)
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McKenzie Formation (2)
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Racine Dolomite (5)
-
Waldron Shale (2)
-
-
Niagaran (43)
-
Upper Silurian
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Cayugan (2)
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Ludlow (12)
-
Pridoli (2)
-
Salina Group (7)
-
-
-
upper Paleozoic
-
Antrim Shale (1)
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Bakken Formation (1)
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Kaskaskia Sequence (1)
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-
Wells Formation (1)
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-
Phanerozoic (20)
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Precambrian
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Archean
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J-M Reef (1)
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Neoarchean (4)
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Central Rand Group (4)
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Stillwater Complex (2)
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upper Precambrian
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Proterozoic
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Damara System (1)
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Mesoproterozoic (2)
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Neoproterozoic
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Ediacaran (3)
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Tonian (1)
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Vendian (4)
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Paleoproterozoic
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Rustenburg Layered Suite (1)
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Ventersdorp Supergroup (3)
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Witwatersrand Supergroup (1)
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igneous rocks
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igneous rocks
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picrite (1)
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anorthosite (2)
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diorites
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tonalite
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gabbros
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norite (1)
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granites (2)
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chromitite (3)
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pyroxenite
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volcanic rocks
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pyroclastics
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volcanic ash (1)
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metamorphic rocks
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minerals (9)
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orthosilicates
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garnet group (2)
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sheet silicates
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chlorite group
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clay minerals
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illite (2)
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sulfates
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Primary terms
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GeoRef Categories
Era and Period
Epoch and Age
Book Series
Date
Availability
reefs
Biological control of ultra-skeleton mineralization in coral
Post-Devonian re-emergence and demise of stromatoporoids as major reef-builders on a Carboniferous Panthalassan seamount
Submarine geomorphology of a glaciated active margin, British Columbia, Canada
Prolonged and gradual recovery of metazoan-algal reefs following the end-Permian mass extinction
Reconstructing past disturbance in coral communities using U-Th dating of dead coral skeletons
Three common sampling techniques in Pleistocene coral reefs of the Red Sea: a comparison
Abstract Line Intercept Transects (LIT), Point Intercept Transects (PIT) and Photoquadrats (PQ) are the most common quantitative sampling techniques in modern and fossil coral reefs. Data from coral reefs obtained by the different methods are generally compared between various reef ages and localities. Quaternary reefs from warmer interglacial periods, which represent climate scenarios projected for the future, are particularly interesting for comparisons with modern reefs. Importantly, fossil reefs differ from modern reefs because they are diagenetically altered and time-averaged. While several studies have compared different quantitative methods in modern reefs, very few have dealt with the comparability among fossil and between fossil and modern reefs. Here, we compare LIT, PIT at 10, 20 and 50 cm intervals and PQ in two Pleistocene reef localities in Egypt. We find that alpha diversity, reef cover and community composition are dependent on the method. Results gained with plotless methods (LIT, PIT) differ strongly from results gained with plot methods (PQ). However, coral cover results are similar with LIT and PIT, and community composition is indistinguishable between the two, but alpha diversity depends on the interval used for PIT. We discuss the implications of our findings for comparing coral reefs of various ages and localities. We recommend surveying Pleistocene reefs with PIT at 20 cm intervals. This is because (1) alpha diversity is well captured, (2) the amount of time-averaging recorded by PIT is reduced compared to PQ, (3) the PIT results can be directly compared to reefs analysed by LIT and (4) the method is less time-consuming than LIT and PQ.
Fossil Java Sea corals record Laurentide ice sheet disappearance
Characteristics and genesis of reef-bank complexes in deep shelf facies: A case study of the Middle-Late Jurassic in the northern Amu Darya Basin, Central Asia
Seismic-based paleoenvironmental analysis of the Paleocene carbonate shelf in Ajdabiya Trough, north-central of Libya
Lagoon infilling by coral reef sand aprons as a proxy for carbonate sediment productivity
Abstract Coastal ecosystems consist of diverse habitats, such as reed beds, salt marshes, mangrove swamps, tidal flats, river deltas, seagrass fields, coral reefs, sandy/rocky-shore beaches and other habitats that harbour biodiversity. The Great East Japan Earthquake of March 2011 caused severe damage to one-third of the fishing communities along the Pacific Ocean of NE Japan. Coastal species, such as seagrasses, function as nursery areas for commercially important species. Coastal ecosystems provide natural infrastructure for the prevention and reduction of hazardous events, a process known as ecosystem-based disaster risk reduction (Eco-DRR). The preparation of topographic and thematic maps of coastal marine environments is essential to establish and visualize the concept of Eco-DRR. Experience gained following the Japanese earthquake, as well as examples from Indonesia and Thailand in the wake of 2004 Indian Ocean tsunami, showed that Eco-DRR is an affordable and sustainable approach. Dissemination of habitat maps should be further promoted as a way to ‘Build Back Better’. To scale up and promote Eco-DRR, scientists must work in a transdisciplinary manner and engage with society by understanding the roles of ecosystems by monitoring and analysing, providing solutions and raising the awareness of community and policy makers, enabling them to better implement Eco-DRR.
Backthrust play of the Chernyshev swell, Timan-Pechora Basin: Reentry into a legacy exploration site based on multidisciplinary study
Time-lapse borehole gravity imaging of CO 2 injection and withdrawal in a closed carbonate reef
ABSTRACT Barbados is actively rising in the latest phase of a long history of emergence that began as far back as 15 Ma. The current phase began at or before ca. 700 ka, is highly nonuniform, and at least locally, has been nonsteady. The uplift rate field in SE Barbados ranges between near-zero and 0.47 m/k.y. and is harmonic to active structures of NNW-SSE contraction. Emergence markers include limestone strata, coral, and shoreline angles, but we used only shoreline angles in calculations. We divided the capping limestone of windward Barbados into 10 units using physical criteria and dated them with over 40 230 Th ages as oxygen isotope stages 5a, 5e, late 7 and early 7, and old (older than 300 ka). The oldest unit is a relic of an earlier phase of emergence. Younger units, probably as old as 700 ka, downlap the eroded flank of the oldest unit and sublimestone foundation. Younger units comprise landward clastic facies deposited on abrasion platforms during eustatic highstand and seaward-coalescent fringe reef blankets deposited on preexisting slopes, mainly in transgression. Earlier models of ridged reefs of catch-up growth origin are not supported in windward Barbados. Shoreline angles, the updip tips of terrace floors and of younger limestone units, are isochronous markers of maximum highstand levels. Despite the lack of direct determination of their ages, shoreline angles provide the truest measures and highest values of emergence. Coral thought to indicate highstand growth gives moderately lower uplift rates due to depths of growth and collapse. Coral grown during transgression gives a marked error in emergence.
ABSTRACT This chapter presents geological documentation of Quaternary (and perhaps older) event histories of southeastern Barbados. The Barbados Limestone is herein formally defined. A time-stratigraphic division of the Barbados Limestone in southeastern Barbados and the properties of the stratigraphic units are presented. A major finding of this study is that the marine terraces originated wholly by marine erosion, not by reef construction, and evolved in stages over a long duration. The hydrology and thickness data of the Barbados Limestone are discussed, and hypotheses on causes of thickness variations are given. The study domain is divided into seven areas that contain a continuous flight of nine marine terraces preserved in various partial sequences. Discussions of these key seven areas in southeastern Barbados are supported by geologic maps at large scale and cross sections. Sections with VE > 1 display limestone stratigraphy and facies over relatively large lengths. Sections with VE = 1 show true structural configurations over short lengths. Detailed observations and radio isotopic dating of the limestone units permit differentiation and correlation among them.
Emergence and Evolution of Barbados is a three-part analysis of the Quaternary geologic and geomorphologic evolution of the island of Barbados in the southeastern Caribbean. “Geology of Southeastern Barbados” assembles and integrates detailed observations into a complex 700 k.y. history of marine sculpting and riverine flooding processes. “Marine Terrace Evolution of Windward Barbados” revises the Quaternary stratigraphy of the island, describes the tectonics of emergence, and demonstrates that uplift rates vary by location. “Active Emergence, Chronology, and Limestone Facies in Southeastern Windward Barbados” is the first comprehensive study to integrate marine erosion and deposition with tectonic uplift rates. Major findings of this work are that Barbados’ Central Highlands are an erosional remnant, and that terraces originated principally by marine erosion rather than by reef construction.
Fringe or background: Characterizing deep-water mudstones beyond the basin-floor fan sandstone pinchout
Shelf-edge delta and reef development on a mixed siliciclastic–carbonate margin, central Great Barrier Reef
Hybrid Nature of the Platinum Group Element Chromite-Rich Rocks of the Norilsk 1 Intrusion: Genetic Constraints from Cr Spinel and Spinel-Hosted Multiphase Inclusions
Abstract The Loyalty Ridge lies to the east and NE of the Norfolk Ridge. The three main Loyalty Islands (Maré, Lifou and Ouvéa) emerge from the ridge at the same latitude as Grande Terre. The islands are uniformly composed of carbonate deposits, except for Maré, where Middle Miocene intra-plate basalts and associated volcaniclastic rocks form restricted outcrops. Miocene rhodolith limestones constitute the bulk of the carbonate cover of the three islands. On Maré, these platform accumulations are locally topped by a dolomitic hardground, which, in turn, is covered by Pliocene–Pleistocene coral-bearing formations. These coral reef constructions are preserved as elevated rims over all three islands and define an atoll stage in their development. The Pleistocene–Holocene palaeoshoreline indicators include fringing bioconstructions and marine notches and record both eustatic sea-level changes and tectonic deformation. The ridge has been in the forebulge region in front of the active Vanuatu subduction zone since the Pliocene and each of the three islands has been uplifted and tilted to varying degrees. Offshore, the Loyalty Ridge continues northwards to the d'Entrecasteaux Zone and southwards to the Three Kings Ridge. Although typically volcanic, the nature of the deep Loyalty Ridge remains unknown.