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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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North America
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Denali Fault (4)
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Tanana River (2)
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Tintina Fault (1)
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Yukon-Tanana Upland (1)
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United States
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Alaska
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Alaska Range (3)
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Delta River (5)
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Fairbanks Alaska (1)
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Susitna River (1)
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Trans-Alaska Pipeline (1)
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fossils
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Invertebrata
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Protista
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Foraminifera
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Fusulinina
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Fusulinidae (1)
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microfossils
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Fusulinina
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Fusulinidae (1)
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geologic age
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Cenozoic
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Quaternary
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Holocene (1)
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Pleistocene (1)
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upper Quaternary (1)
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Tertiary
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Neogene
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Pliocene (1)
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Paleozoic
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Permian (1)
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Primary terms
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Cenozoic
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Quaternary
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Holocene (1)
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Pleistocene (1)
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upper Quaternary (1)
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Tertiary
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Neogene
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Pliocene (1)
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deformation (1)
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earthquakes (2)
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engineering geology (1)
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faults (4)
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geomorphology (1)
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geophysical methods (1)
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Invertebrata
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Protista
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Foraminifera
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Fusulinina
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Fusulinidae (1)
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North America
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Denali Fault (4)
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Tanana River (2)
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Tintina Fault (1)
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Yukon-Tanana Upland (1)
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paleogeography (1)
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Paleozoic
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Permian (1)
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pollution (1)
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soil mechanics (2)
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stratigraphy (1)
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structural geology (1)
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tectonics
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neotectonics (1)
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United States
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Alaska
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Alaska Range (3)
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Delta River (5)
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Fairbanks Alaska (1)
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Susitna River (1)
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Trans-Alaska Pipeline (1)
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sedimentary structures
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channels (1)
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Delta River
Geomorphic evidence of active transpressional deformation in the Tanana foreland basin, south-central Alaska
Geomorphic data from rivers in the Tanana foreland basin and northern foothills of the Alaska Range indicate that this is an actively deforming landscape. The Tanana basin is an alluvial and swampy lowland of ∼22,000 km 2 located in south-central Alaska between the northern flank of the Alaska Range and the Yukon-Tanana uplands. The major axial drainage of the basin is the Tanana river, which is fed by large transverse braided rivers flowing northward out of the Alaska Range. To better define active structures and the neotectonic configuration of the basin, we have constructed a series of longitudinal stream profiles along the major rivers of the Tanana basin. Stream profiles along with changes in channel morphologies delineate four main areas of active deformation. (1) In the western part of the basin, major rivers in the Kantishna Hills area have stream profiles and changes in channel morphologies that indicate that the northeast-trending Kantishna Hills anticlinorium is an active structure. All longitudinal stream profiles in this area exhibit convexity, suggesting tectonic perturbation, as they cross the trend of this 85-km-long structure. In addition, the channel of the McKinley River clearly becomes entrenched as it flows around the southwestern nose of the Kantishna Hills anticlinorium suggesting that the structure may be propagating southwestward. Our geomorphic data from this area are consistent with well-documented seismicity along the southwestern part of the Kantishna Hills. (2) In the central part of the basin, the Nenana River area, changes in channel morphology, stream profile perturbations, and uplifted Pliocene-Pleistocene erosional surfaces coincide with a series of east-trending anticlines. We interpret these folds as part of an active Neogene thrust belt that forms the foothills of the north-central Alaska Range. This active thrust belt is propagating northward and deforming the proximal part of the Tanana foreland basin. North of the topographic front of the foothills, stream profiles indicate active subsidence of the basin. (3) In the eastern part of the Tanana basin, the Delta River area, stream profiles and channel morphologies delineate active deformation along the strike-slip Denali fault and the Granite Mountain/Donnelly Dome thrust fault system. (4) In the northern part of the Tanana basin, the Fairbanks area, stream profiles and channel morphologies delineate northeast-trending active structures that coincide with known seismic zones. These structures are most likely related to block rotation between the Denali and Tintina fault systems along northeast-trending sinistral strike-slip faults. An interesting result of our analysis of the Fairbanks area is the hypothesis that the Tanana River has been forced to abandon its previous channels due to progressive uplift along an active northeast-trending structure. This forced migration has resulted in a series of watergaps, with the modern Tanana River having been deflected around the southwestern culmination of this structure. Interactions between fluvial systems and active structures of the Tanana basin provide a surface record of regional transpressional deformation. This deformation is accommodated by strain partitioning between strike-slip faults like the Denali fault, an active thrust belt along the northern flank of the Alaska Range, and rotation of crustal blocks between the Denali and Tintina fault systems.
Geotechnical Reconnaissance of the 2002 Denali Fault, Alaska, Earthquake
Trans-Alaska Pipeline System Performance in the 2002 Denali Fault, Alaska, Earthquake
Evidence for Quaternary Movement on the McKinley Strand of the Denali Fault in the Delta River Area, Alaska
Biostratigraphy and Lower Permian Fusulinidae of the Upper Delta River Area, East-Central Alaska Range
A Lower Permian fusulinid fauna was found in rocks of Mankomen age within a fault block in the Upper Delta River area, east-central Alaska Range. Three members of the M ankomen Formation are recognized and described from this area. They are, in stratigraphic order: a lower Tuffaceous Sandstone Member, an Alternating Limestone-Shale Member, and a Limestone Member. Additional sedimentary rocks occur still higher in the section but are as yet unmapped. The section exposed in this area represents the youngest known Upper Paleozoic sediments in the Alaska Range. Eighteen species of fusulinids belonging to three genera are described from the Alternating Limestone-Shale Member and Limestone Member. They are: Pseudofusulinella valkenburghae n. sp.; P . cf. P. parvula Skinner and Wilde; P. sp. A; Eoparafusulina mendenhalli n. sp.; E. waddelli n. sp.; Schwagerina pseudokaragasensis n. sp.; S. cf. S. emaciata (Beede); S. sp. A; S. rowetti n. sp.; S. callosa (Rauser-Chernousova); S. whartoni n. sp.; S. heineri n. sp.; S. moffiti n. sp.; S. sp. B; S. sp. C; S. rainyensis n. sp.; S. mankomenensis n. sp.; and S. hyperborea (Salter). This fauna is divided into six assemblage zones on the basis of the fusulinid species. Collectively, the zones indicate a Lower Permian age, ranging from late Asselian to middle Artinskian when compared to the zonation of Permian sections in the western Urals, USSR. The fusulinids from the Lower Permian of the Alaska Range belong to the Boreal faunal realm that includes the geosynclinal seas of the Alaskan Cordilleran, Franklinian, and Uralian geosynclines. Faunal evidence indicates temporary marine connections between Alaska and the Pacific north-west, and between the Uralian and Tethyan regions. Correlations are suggested between the Alaska Range section and the following regions: southeastern Alaska; northeastern Alaska; northwestern Yukon Territory; Grinnell Peninsula, Arctic Archipelago; northwest Greenland; Spitsbergen; and the Ural region of the USSR.