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NARROW
GeoRef Subject
-
all geography including DSDP/ODP Sites and Legs
-
Africa
-
Central Africa
-
Angola (1)
-
-
North Africa
-
Atlas Mountains
-
Moroccan Atlas Mountains
-
High Atlas (1)
-
-
-
Egypt (1)
-
Maghreb (1)
-
Morocco
-
Moroccan Atlas Mountains
-
High Atlas (1)
-
-
Rif (1)
-
-
-
Southern Africa
-
Karoo Basin (1)
-
South Africa (1)
-
-
West Africa
-
Nigeria
-
Niger Delta (3)
-
-
-
-
Altiplano (2)
-
Arctic Ocean
-
Barents Sea (3)
-
-
Arctic region
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Greenland
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East Greenland (1)
-
Northern Greenland (1)
-
-
Svalbard
-
Spitsbergen (2)
-
-
-
Asia
-
Arabian Peninsula
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Oman
-
Oman Mountains (1)
-
-
-
Far East
-
Borneo
-
Brunei (1)
-
Kalimantan Indonesia
-
Mahakam Delta (1)
-
-
-
China
-
Qinghai China (1)
-
Sichuan Basin (1)
-
Xinjiang China (1)
-
Xizang China (1)
-
-
Indonesia
-
Kalimantan Indonesia
-
Mahakam Delta (1)
-
-
-
Lesser Sunda Islands
-
Timor (2)
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Taiwan
-
Chelungpu Fault (1)
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Himalayas
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High Himalayan Crystallines (1)
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Kumaun Himalayas (1)
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Lesser Himalayas (3)
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Indian Peninsula
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India
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Nepal (2)
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Pakistan
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Main Central Thrust (2)
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Australasia
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Ionian Zone (1)
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Malay Archipelago
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Borneo
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Brunei (1)
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Kalimantan Indonesia
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Mahakam Delta (1)
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-
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New Guinea (1)
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Timor (2)
-
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Mediterranean region
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Ionian Islands
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Cephalonia (1)
-
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Mediterranean Sea
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East Mediterranean
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Adriatic Sea (1)
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Black Sea (3)
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Hellenic Trench (1)
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Mexico
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Campeche Mexico (1)
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Guerrero Mexico (1)
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Mexico state
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Michoacan Mexico (1)
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Puebla Mexico (1)
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-
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North America
-
Appalachian Basin (1)
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Appalachians
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Blue Ridge Mountains (2)
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Basin and Range Province
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Pacific Ocean
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North Pacific
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Gulf of Alaska (1)
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South Pacific
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West Pacific
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Puna (2)
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Subandean Belt (4)
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Argentina
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Cherokee County Georgia (1)
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Montana
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Humboldt Range (1)
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New Mexico
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Pennsylvania
-
Lackawanna County Pennsylvania (1)
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Sevier orogenic belt (3)
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commodities
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mineral deposits, genesis (3)
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elements, isotopes
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metals
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neodymium
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fossils
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Invertebrata
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microfossils
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geochronology methods
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thermochronology (3)
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geologic age
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Cenozoic
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Siwalik System (1)
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Tertiary
-
Anahuac Formation (1)
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Neogene
-
Ipururo Formation (1)
-
Miocene
-
lower Miocene (3)
-
middle Miocene
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upper Miocene
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-
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Pliocene (2)
-
-
Paleogene
-
Claron Formation (1)
-
Eocene
-
upper Eocene (2)
-
-
Oligocene
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Frio Formation (1)
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lower Oligocene (1)
-
-
Paleocene
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middle Paleocene (1)
-
-
-
upper Tertiary (1)
-
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upper Cenozoic (1)
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Mesozoic
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Cretaceous
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Lower Cretaceous
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Upper Cretaceous
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Senonian (3)
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Straight Cliffs Formation (1)
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-
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Jurassic
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lower Liassic (1)
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Nugget Sandstone (1)
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Vaca Muerta Formation (1)
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Paleozoic
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Arbuckle Group (2)
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Lower Cambrian
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Rome Formation (1)
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-
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Carboniferous
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Mississippian (4)
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Lower Pennsylvanian
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Morrowan (1)
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Pottsville Group (1)
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Upper Pennsylvanian
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Virgilian (1)
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-
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Upper Carboniferous (1)
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Devonian
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Middle Devonian
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Hamilton Group (1)
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Ramparts Formation (1)
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Knox Group (1)
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lower Paleozoic (2)
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middle Paleozoic (1)
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Ordovician
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Upper Ordovician (1)
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Permian
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Ecca Group (1)
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Lower Permian
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Leman Sandstone Formation (1)
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Middle Permian (1)
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Phosphoria Formation (1)
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Upper Permian
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Zechstein (1)
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-
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Silurian
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Middle Silurian (1)
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Upper Silurian
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Salina Group (1)
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-
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upper Paleozoic (3)
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-
Precambrian
-
Archean
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Paleoarchean (1)
-
-
Prince Albert Group (1)
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upper Precambrian
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Proterozoic
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Mesoproterozoic
-
Belt Supergroup (1)
-
-
Neoproterozoic (4)
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Paleoproterozoic
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Svecofennian (1)
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-
-
-
-
-
igneous rocks
-
igneous rocks
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plutonic rocks
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diorites (1)
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granites (2)
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pegmatite (1)
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volcanic rocks
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trachytes (1)
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-
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ophiolite (2)
-
-
metamorphic rocks
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metamorphic rocks
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amphibolites (1)
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gneisses
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augen gneiss (1)
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orthogneiss (1)
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metaigneous rocks
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metasedimentary rocks (3)
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ophiolite (2)
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turbidite (2)
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minerals
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carbonates
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calcite (1)
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oxides
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phosphates
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apatite (3)
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monazite (1)
-
-
silicates
-
chain silicates
-
amphibole group
-
clinoamphibole
-
hornblende (1)
-
-
-
-
orthosilicates
-
nesosilicates
-
zircon group
-
zircon (3)
-
-
-
-
ring silicates
-
emerald (1)
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-
sheet silicates
-
clay minerals
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smectite (1)
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illite (2)
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mica group
-
biotite (2)
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-
-
-
sulfides (1)
-
-
Primary terms
-
absolute age (10)
-
Africa
-
Central Africa
-
Angola (1)
-
-
North Africa
-
Atlas Mountains
-
Moroccan Atlas Mountains
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High Atlas (1)
-
-
-
Egypt (1)
-
Maghreb (1)
-
Morocco
-
Moroccan Atlas Mountains
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High Atlas (1)
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Rif (1)
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-
-
Southern Africa
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Karoo Basin (1)
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South Africa (1)
-
-
West Africa
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Nigeria
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Niger Delta (3)
-
-
-
-
Arctic Ocean
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Barents Sea (3)
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-
Arctic region
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Greenland
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East Greenland (1)
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Northern Greenland (1)
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Svalbard
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Spitsbergen (2)
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Asia
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Arabian Peninsula
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Oman
-
Oman Mountains (1)
-
-
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Far East
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Borneo
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Brunei (1)
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Kalimantan Indonesia
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Mahakam Delta (1)
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-
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China
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Xinjiang China (1)
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Xizang China (1)
-
-
Indonesia
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Kalimantan Indonesia
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Mahakam Delta (1)
-
-
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Lesser Sunda Islands
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Timor (2)
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Taiwan
-
Chelungpu Fault (1)
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Himalayas
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Indian Peninsula
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India
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Nepal (2)
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Pakistan
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Punjab Pakistan
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Sulaiman Range (1)
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Potwar Plateau (1)
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Main Central Thrust (2)
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Middle East
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Iran
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Elburz (1)
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Iraq
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Syria (1)
-
Zagros (3)
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thin-skinned tectonics
A Thermal Profile across the Idaho-Montana Fold-Thrust Belt Reveals a Low-Relief Orogenic Wedge That Developed atop a Pre-Orogenic Basement High
The 2020 M w 6.0 Jiashi Earthquake: Coinvolvement of Thin‐Skinned Thrusting and Basement Shortening in Shaping the Keping‐Tage Fold‐and‐Thrust Belt in Southwestern Tian Shan
Structural geometry and evolution of the Carter-Knox structure, Anadarko Basin, Oklahoma
Structural analysis of the Wichita Uplift and structures in the Anadarko Basin, Southern Oklahoma
A structural analysis of the Washita Valley Fault in the southeast Anadarko Basin
The enigma of the Albian Gap: spatial variability and the competition between salt expulsion and extension
Four-dimensional analog and geometrical modeling of the Hides anticline, Papua New Guinea: Structure of a giant gas field
Abstract The outer parts of collision mountain belts are commonly represented by fold and thrust belts. Many of the key concepts in the structural geology of fold and thrust belts have origins in ancient orogens such as the Appalachians and Caledonian chains of Europe, together with the Alps. Impetus in thrust belt research then came from the desire to exploit geological resources that reside in the subsurface, especially arising from hydrocarbon exploration in the foothills of the Canadian Cordillera in the 1960s and 1970s. Notwithstanding decades of exploitation, continental fold and thrust belts are still estimated to hold reserves of 700 billion barrels of oil equivalent. But exploration will focus increasingly on small, hard-to-resolve structures. Basic geological understanding remains as important today as it did for the pioneering explorers in the Canadian foothills. It is a theme that runs throughout this Special Publication.
Abstract In 1888, inspired by fieldwork in what has become known as the Moine Thrust Belt, NW Scotland, Henry Cadell conducted a pioneering series of analogue deformation experiments to investigate the structural evolution of fold–thrust belts. Some experiments showed that imbricate thrusts build up thrust wedges of variable form, without requiring precursor folding. Others demonstrated a variety of fold–thrust structures and how heterogeneities in basement can localize thrust structures. These experiments are described here and used to draw lessons on how analogue deformation experiments are used to inform the interpretation of fold–thrust structures. Early adopters used Cadell's results as guides to structural styles when constructing cross-sections in thrust belts. His models and the host of others created since serve to illustrate part of the range of structural geometries in thrust belts. However, as with much subsequent work, Cadell's use of a deformation apparatus, with a fixed basal slip surface, biases perceptions of fold–thrust belts to be necessarily ‘thin-skinned’ (experimental design bias) and can simply reinforce established interpretations of natural systems (confirmation bias). So analogue deformation experiments may be unreliable guides to the deterministic interpretations of specific fold–thrust structures in the sub surface of the real world.
Abstract A detailed analysis of the Late Miocene Mandach Thrust, a key tectonic structure of the easternmost Jura Mountains (northern Alpine foreland), is presented providing insights into the modes of along-strike structural cover–basement interactions in a classical foreland setting. Our study builds on the construction, restoration and forward modelling of eight closely spaced cross-sections constrained by depth-migrated 2D seismics and geological maps. The results indicate predominantly thin-skinned thrust tectonics without significant inversion of underlying basement structures. However, inherited pre-thrusting normal faults exerted a strong control on the observed thrusting style, changing along-strike from a comparatively simple geometry to a complex, partly overthrust, partly reactivated normal fault. The observed variations relate to changes in the relief of the mechanical basement and the characteristics of pre-thrusting normal faults. The thrust's complexity is further increased by the local activation of secondary detachment horizons and possibly along-strike sedimentary facies changes within the thrust-faulted sedimentary sequence. The variations in thrusting style go along with subtle changes in shortening that may point towards as yet undetected transfer structures. As such, our structural analysis of the Mandach Thrust provides an improved understanding of the fault's kinematics and serves to highlight existing exploration uncertainties.
Abstract We defined the folding sequence of the fold–thrust belt of the Western Papua New Guinea Highlands by analysing the surface expression of the structures and the response of the drainage system to the active fold–thrust belt. The interaction between structures is typically assessed by examining the syn-kinematic strata preserved; however, in our study area, this is problematic as these strata are poorly imaged on seismic lines. This study found common morphological features that allowed grouping and mapping of three different structural settings: group I, basement-involved tectonics; group II, thin-skinned anticlines which sole near the Koi–Iangi Sandstone; and group III, thin-skinned folds associated with the intra-Ieru Formation detachment. Fold Front Sinuosity analysis supports the idea that the fold–thrust belt propagates from the NW to the SE. Considering the detailed morphotectonics and drainage analyses, we interpret that the group II folds developed as out-of-sequence thrusting and folding, associated with buttressing against the group I larger structures.
Geological development of the Timor Orogen
Abstract The Timor Orogen comprises the island of Timor, a narrow offshore area to the north and a wider offshore fold-and-thrust belt to the south. This orogen formed by jamming and subsequent collision of the Banda Sea subduction system by the Australian Plate. The BandaSeis seismic survey has revealed excellent images of the deep-water fold-and-thrust belt. Seismic interpretation of the dataset demonstrated structural and tectonic features not previously described, including regional geological features on the Australian continental crust and two regional NE–SW sinistral strike-slip faults, and a prominent Middle Permian palaeogeographical high (Timor Plateau). Moreover, since the Middle–Late Triassic and Middle Jurassic, the two NE-trending strike-slip faults governed the formation of the West Timor and Cova-Lima sub-basins. The location along the Australian margin plays a dominant role in controlling the structural style and shaping of the Timor Orogen. Vertical loading and the southerly motion of the orogenic wedge are the main driving forces responsible for its building, illustrating a thin-skinned tectonic framework. Thrust faults nucleate in a forward-breaking sequence in the motion of thrust transport, with younger thrusts developing in front of older thrusts. Most of the collisional deformation has been classified into two styles: shallow thin-skinned and deep-seated deformation.
Paleomagnetic and magnetic fabric data from Lower Triassic redbeds of the Central Western Carpathians: new constraints on the paleogeographic and tectonic evolution of the Carpathian region
Progressive tilting of salt-bearing continental margins controls thin-skinned deformation
Abstract The tectonic framework of NW Himalaya is different from that of the central Himalaya with respect to the position of the Main Central Thrust and Higher Himalayan Crystalline and the Lesser and Sub Himalayan structures. The former is characterized by thick-skinned tectonics, whereas the thin-skinned model explains the tectonic evolution of the central Himalaya. The boundary between the two segments of Himalaya is recognized along the Ropar–Manali lineament fault zone. The normal convergence rate within the Himalaya decreases from c. 18 mm a −1 in the central to c. 15 mm a −1 in the NW segments. In the last 800 years of historical accounts of large earthquakes of magnitude M w ≥ 7, there are seven earthquakes clustered in the central Himalaya, whereas three reported earthquakes are widely separated in the NW Himalaya. The earthquakes in central Himalaya are inferred as occurring over the plate boundary fault, the Main Himalayan Thrust. The wedge thrust earthquakes in NW Himalaya originate over the faults on the hanging wall of the Main Himalayan Thrust. Palaeoseismic evidence recorded on the Himalayan front suggests the occurrence of giant earthquakes in the central Himalaya. The lack of such an event reported in the NW Himalaya may be due to oblique convergence.