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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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Atlantic Ocean (1)
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Mexico
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Mexico
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United States
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Massachusetts
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Texas
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sediments
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gravel (1)
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mud (1)
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soils
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paleosols (3)
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soils
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Vertisols (2)
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Eolian sedimentation and soil development on a semiarid to subhumid grassland, Tertiary Ogallala and Quaternary Blackwater Draw formations, Texas and New Mexico High Plains
Lithostratigraphy and geochronology of fills in small playa basins on the Southern High Plains, United States
Origin of satin spar veins in evaporite basins
Caulerpa-like marine alga from Permian strata, Palo Duro Basin, West Texas
Buried Vertisols in lacustrine facies of the Pliocene Fort Hancock Formation, Hueco Bolson, West Texas and Chihuahua, Mexico
Quaternary geology of the Southern Great Plains and an adjacent segment of the Rolling Plains
Abstract The Southern Great Plains physiographic sub-province lies south of the Cimarron River, which crosses the plains at ~37° N latitude (Fig. 1). The sub-province is bounded on the west by the Southern Rocky Mountains Province and Sacramento section of the Basin and Range Province. On the east the Great Plains are bounded by the Caprock Escarpment and are separated from the Gulf Coastal Plain by the Balcones Escarpment. The southern Great Plains physiographic sub-province is divided into the Pecos Valley and Raton sections on the west, the High Plains section on the east, and the Edwards Plateau on the south. “In the public mind the Great Plains are thought of as a vast monotonous plain that lacks scenic interest, but has to be crossed to reach the scenic Rocky Mountains to the west“ (Thornbury, 1965, p. 287). Whereas this region clearly lacks areas of high relief and thus scenic wonders, it does contain some of the most extensive deposits of Tertiary and Quaternary sedimentary and volcanic rocks that have been recognized in North America. These units are commonly well exposed along the banks of stream systems being incised into the Great Plains and in the high scarps that bound the High Plains. Numerous descriptions of the Quaternary geology and geomorphology of the Southern Great Plains have been published since the first reports became available late in the 19th and early 20th centuries (Johnson, 1901; Baker, 1915). Of these, useful reviews or
Depositional facies of the Miocene-Pliocene Ogallala Formation, northwestern Texas and eastern New Mexico
A depositional model for outwash, sediment sources, and hydrologic characteristics, Malaspina Glacier, Alaska: A modern analog of the southeastern margin of the Laurentide Ice Sheet
Regional Hydrogeologic Research in the Palo Duro Basin for Nuclear-Waste Repository Siting
Great Plains
Abstract The Great Plains Physiographic Province (Fig. 1) is a generally north-south band of the western interior of North America, subcontinental in scale, that averages about 600 km in width and extends from northwestern Canada through the United States to the border with Mexico. With tongue-in-cheek, Thornbury (1965, p. 287) claimed that “in the public mind the Great Plains are thought of as a vast monotonous plain that lacks scenic interest, but has to be crossed to reach the scenic Rocky Mountains to the west.” It is generally true that the Great Plains, and especially the High Plains, have low relief. But there are many scenic exceptions, largely areas of negative relief along the eroded margins of the plains and in river valleys. Areas of positive relief include structural highs such as the Black Hills (Fig. IB) and other outliers of the Rocky Mountains. These areas of positive and negative relief are especially important, because they contain the sections where the geologic and geomorphic history of the Great Plains is best exposed.
Geomorphic development of the Canadian River Valley, Texas Panhandle: An example of regional salt dissolution and subsidence
Structural influences on geomorphic processes and physiographic features, Texas Panhandle: Technical issues in siting a nuclear-waste repository
Retreat of the Caprock Escarpment and Denudation of the Rolling Plains in the Texas Panhandle
Paleotemperature analysis of the marine Pleistocene of Long Island, New York, and Nantucket Island, Massachusetts: Discussion and reply: Reply
Paleotemperature analysis of the marine Pleistocene of Long Island, New York, and Nantucket Island, Massachusetts
Bathymetry and sediment distribution in proglacial Malaspina Lake, Alaska
Sedimentation and Physical Limnology in Proglacial Malaspina Lake, Southeastern Alaska
Abstract Malaspina Lake is a large proglacial lake which lies along the southeastern margin of the Malaspina Glacier, Alaska. It is density stratified with respect to suspended sediment content, which ranges from 0.1 grams per liter at the surface to 0.7 grams per liter at a depth of 45 m. The lake is not thermally stratified since water near the temperature of its maximum density (3.94°C) occurs close to the lake surface and water as cold as 0.3°C occurs at the lake bottom. Two large surface streams, Russell Stream and Tarr Stream, flow into the lake, and their combined discharge was measured at 140 cubic meters per second. Discharge from the lake ranged from 490 cubic meters per second to 600 cubic meters per second, and thus subglacial and englacial streams were apparently discharging as much as 460 cubic meters per second into the lake. Tarr Stream, which loses suspended sediment in a series of small lakes that act as settling basins, enters the lake as an overflow. Russell Stream and Tunnel Stream, which is an englacial stream, are both highly charged with suspended sediment and enter the lake as continuous turbidity currents or underflows. Two underflows and two interflows were recorded along the ice-contact margin of the lake. These underflows and interflows apparently originate from englacial or subglacial streams discharging into Malaspina Lake. Bottom topography of the lake is quite irregular except where the selective infilling of basins by turbidity currents has produced flat to gently sloping topography. Cores taken from these flat areas contain varved sediments. Varves, deposited at depths of SO m or more, contain numerous normal and reverse graded beds. The current-bedded portion of the varve was deposited from an underflow or turbidity current. The varve was completed by the deposition of a clay unit from suspension when continuous underflows, or turbidity currents, ceased during the winter months.
Depositional Sequences in Glaciolacustrine Deltas
Abstract Sedimentary structures in distal outwash deposits, in glaciolacustrine deltas, and in lake sediments proximal to glaciolacustrine deltas are similar where the grain-size distributions of the sediment are similar, and where depositon occurs under smilar flow conditions. Draped lamination, a common structure in distal outwash deposit, consists of parallel laminae of sand, silt, and clay deposited from suspension and draped over an underlying bedform. Thickness of the laminae remains essentially unchanged across the underlying bedform, and neither silt nor mica flakes are concentrated anywhere along draped laminae. Overbank deposits in outwash decrease in grain size along the length of the stream, but contain similar sequences of sedimentary structures. Commonly, type A ripple-drift cross-lamination is overlain by low-angle type B, which in turn is overlain by draped lamination. This sequence of sedimentary structures suggests deposition under decreasing flow strength. Ripple-drift sequences in glaciolacustrine deltas are separated in many cases by winter clay layers. The basic sequence begins as a thin unit of draped lamination deposited on a subjacent winter clay. A thin unit of type B ripple-drift cross-lamination follows and is in turn overlain by a relatively thick unit of type A. The type A grades upward into a second unit of type B. As the angle of climb of the type B ripple-drift cross-lamination increases to the vertical, type B grades upward into draped lamination. A superjacent winter clay layer completes the sequence. The basic sequence of sedimentary structures reflects a relatively rapid decrease in the ratio of rates of deposition from suspension to bed-load transport, followed by a gradual increase. Flow strength appears to increase quickly and then decrease. The thin graded beds and rare ripple- drift cross-lamination or isolated ripples observed within lacustrine varved clays are distal equivalents to the sequences observed within glaciolacustrine deltas. Glaciolacustrine deltas are the products of rapid sedimentation into low-energy lake environments and are seldom seriously modified by wave action or currents. Deltas are built into lakes as overlapping lobes of sediment that were deposited from density currents issuing from meltwater distributaries. As distributaries migrate across the delta subaerial plain, lobes move laterally and overlap each other, forming an arcuate delta front.