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NARROW
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all geography including DSDP/ODP Sites and Legs
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Australasia
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Late Neogene–Quaternary tephrochronology, stratigraphy, and paleoclimate of Death Valley, California, USA
Evolution of ancient Lake Alamosa and integration of the Rio Grande during the Pliocene and Pleistocene
From Pliocene to middle Pleistocene time, a large lake occupied most of the San Luis Valley above 2300 m elevation (7550 ft) in southern Colorado. This ancient lake accumulated sediments of the Alamosa Formation (Siebenthal, 1910), for which the lake is herein named. The existence of this lake was first postulated in 1822 and proven in 1910 from well logs. At its maximum extent of nearly 4000 km 2 , it was one of the largest high-altitude lakes in North America, similar to but larger than Lake Texcoco in the Valley of Mexico. Lake Alamosa persisted for ~3 m.y., expanding and contracting and filling the valley with sediment until ca. 430 ka, when it overtopped a low sill and cut a deep gorge through Oligocene volcanic rocks in the San Luis Hills and drained to the south. As the lake drained, nearly 100 km 3 (81 × 10 6 acre-ft or more) of water coursed southward and flowed into the Rio Grande, entering at what is now the mouth of the Red River. The key to this new interpretation is the discovery of ancient shoreline deposits, including spits, barrier bars, and lagoon deposits nestled among bays and in backwater positions on the northern margin of the San Luis Hills, southeast of Alamosa, Colorado. Alluvial and lacustrine sediment nearly filled the basin prior to the lake's overflow, which occurred ca. 430 ka as estimated from 3 He surface-exposure ages of 431 ± 6 ka and 439 ± 6 ka on a shoreline basalt boulder, and from strongly developed relict calcic soils on barrier bars and spits at 2330–2340 m (7645–7676 ft), which is the lake's highest shoreline elevation. Overtopping of the lake's hydrologic sill was probably driven by high lake levels at the close of marine oxygen-isotope stage (OIS) 12 (452–427 ka), one of the most extensive middle Pleistocene glacial episodes on the North American continent. Hydrologic modeling of stream inflow during full-glacial-maximum conditions suggests that Lake Alamosa could fill at modern precipitation amounts if the mean annual temperature were just 5 °C (10 °F) cooler, or could fill at modern temperatures with 1.5 times current mean annual precipitation. Thus, during pluvial epochs the lake would rise to successively higher levels owing to sedimentation; finally during OIS 12, the lake overflowed and spilled to the south. The integration of the upper (Colorado) and lower (New Mexico) reaches of the Rio Grande expanded the river's drainage basin by nearly 18,000 km 2 and added recharge areas in the high-altitude, glaciated San Juan Mountains, southern Sawatch Range, and northern Sangre de Cristo Mountains. This large increase in mountainous drainage influenced the river's dynamics downstream in New Mexico through down-cutting and lowering of water tables in the southern part of the San Luis Valley.
During glacial (pluvial) climatic periods, Death Valley is hypothesized to have episodically been the terminus for the Amargosa, Owens, and Mojave Rivers. Geological and biological studies have tended to support this hypothesis and a hydrological link that included the Colorado River, allowing dispersal of pupfish throughout southeastern California and western Nevada. Recent mitochondrial deoxyribonucleic acid (mtDNA) studies show a common pupfish (Cyprinodontidae) ancestry in this region with divergence beginning 3–2 Ma. We present tephrochronologic and paleomagnetic data in the context of testing the paleohydrologic connections with respect to the common collection point of the Amargosa, Owens, and Mojave Rivers in Death Valley during successive time periods: (1) the late Pliocene to early Pleistocene (3–2 Ma), (2) early to middle Pleistocene (1.2–0.5 Ma), and (3) middle to late Pleistocene (<0.7–0.03 Ma; paleolakes Manly and Mojave). Using the 3.35 Ma Zabriskie Wash tuff and 3.28 Ma Nomlaki Tuff Member of the Tuscan and Tehama Formations, which are prominent marker beds in the region, we conclude that at 3–2 Ma, a narrow lake occupied the ancient Furnace Creek Basin and that Death Valley was not hydrologically connected with the Amargosa or Mojave Rivers. A paucity of data for Panamint Valley does not allow us to evaluate an Owens River connection to Death Valley ca. 3–2 Ma. Studies by others have shown that Death Valley was not hydrologically linked to the Amargosa, Owens, or Mojave Rivers from 1.2 to 0.5 Ma. We found no evidence that Lake Manly flooded back up the Mojave River to pluvial Lake Mojave between 0.18 and 0.12 Ma, although surface water flowed from the Amargosa and Owens Rivers to Death Valley at this time. There is also no evidence for a connection of the Owens, Amargosa, or Mojave Rivers to the Colorado River in the last 3–2 m.y. Therefore, the hypothesis that pupfish dispersed or were isolated in basins throughout southeastern California and western Nevada by such a connection is not supported. Beyond the biologically predicted time frame, however, sparse and disputed data suggest that a fluvial system connected Panamint (Owens River), Death, and Amargosa Valleys, which could account for the dispersal and isolation before 3 Ma.
Late Quaternary Paleoseismology of the Southern Steens Fault Zone, Northern Nevada
Paleoseismicity of Two Historically Quiescent Faults in Australia: Implications for Fault Behavior in Stable Continental Regions
Dating methods applicable to the Quaternary
Abstract A wide variety of dating methods are used in Quaternary research, and each method has many applications and limitations. Because of this variety, we cannot discuss the applications and limitations of all methods here. The more versatile and widely used methods, including 14 C, K/Ar, fission-track, U-series, paleomagnetism, thermoluminescence, and amino acid dating are treated more comprehensively in this chapter than other methods that are shown on the summary chart. The summary chart is provided here to give an overview of dating work and research for the Quaternary. This summary consists mainly of a table (Plate 2) that is modified and updated from Colman and Pierce (1977, Plate 1, ref. 66). The table is intended as an overview and concise guide to Quaternary dating methods. It contains many subjective judgments and should not be considered definitive; the entries for applicability, age range, and optimum resolution are particularly interpretive. Details concerning assumptions, analytical techniques, uncertainties, and interpretations should be obtained from specialized references using the key references in Plate 2 as a guide. The dating methods described range from well-known and established techniques to experimental procedures whose results are subject to considerable interpretation. Key references included on Plate 2 are intended as an entry into the vast literature on dating methods; space prohibits a more complete listing. We have emphasized recent review papers and notable examples of applications as sources of additional references and information. Dating methods discussed in other sections of this chapter are indicated by asterisks in.
Quaternary geology of the Colorado Plateau
Abstract The Colorado Plateau differs greatly from its neighboring physiographic provinces, the Rocky Mountains on the north and east, and the Basin and Range Province on the west and south. The Colorado Plateau is a huge (about 384,000 km 2 ), roughly circular region of many high plateaus and isolated mountains that encompasses large parts of Utah, Colorado, New Mexico, and Arizona. The plateau derives its name from the Colorado River, which drains at least 90 percent of its area (Fig. 1). The distinguishing features of the Colorado Plateau are: its considerable altitude, nearly all above 1,500 m; its nearhorizontal bedrock (steeply inclined beds are limited to the few great monoclines and the borders of certain uplifts); and its strong stepped landscapes, consisting of many cliff-like escarpments separated by wide, gentle slopes (the result of differential erosion of the generally flat-lying rocks). The plateau consists of six sections (Fenneman, 1931). Different bedrock stratigraphy and structure have profoundly affected the physiography and geomorphology of each section (Fig. 1). The northern section of the Colorado Plateau consists of the Uinta basin, a broad structural basin bounded on the north by the Uinta Mountains and on the south by the San Rafael swell (Figs. 1 and 2). The east-flowing Duchesne River and the west-flowing White River drain the basin, and both join the south-flowing Green River near Ouray, Utah. The Green River has cut Desolation Canyon where the river flows across the southern rim of the.
Surface faulting accompanying the Borah Peak earthquake and segmentation of the lost river fault, central Idaho
Documentation of benchmark photographs that show the effects of the 1983 Borah Peak earthquake with some considerations for studies of scarp degradation
History of quaternary offset and paleoseismicity along the La Jencia fault, central Rio Grande rift, New Mexico
Calcic soils are commonly developed in Quaternary sediments throughout the arid and semiarid parts of the southwestern United States. In alluvial chronosequences, these soils have regional variations in their content of secondary calcium carbonate (CaCO 3 ) because of (1) the combined effects of the age of the soil, (2) the amount, seasonal distribution, and concentration of Ca ++ in rainfall, and (3) the CaCO 3 content and net influx of airborne dust, silt, and sand. This study shows that the morphology and amount of secondary CaCO 3 (cS) are valuable correlation tools that can also be used to date calcic soils. The structures in calcic soils are clues to their age and dissolution-precipitation history. Two additional stages of carbonate morphology, which are more advanced than the four stages previously described, are commonly formed in middle Pleistocene and older soils. Stage V morphology includes thick laminae and incipient pisolites, whereas Stage VI morphology includes the products of multiple cycles of brecciation, pisolite formation, and wholesale relamination of breccia fragments. Calcic soils that have Stage VI morphology are associated with the late(?) Miocene constructional surface of the Ogallala Formation of eastern New Mexico and western Texas and the early(?) Pliocene Mormon Mesa surface of the Muddy Creek Formation east of Las Vegas, Nevada. Thus, calcic soils can represent millions of years of formation and, in many cases, provide evidence of climatic, sedimentologic, and geologic events not otherwise recorded. The whole-profile secondary CaCO 3 content (cS) is a powerful developmental index for calcic soils: cS is defined as the weight of CaCO 3 in a 1-cm 2 vertical column through the soil (g/cm 2 ). This value is calculated from the thickness, CaCO 3 concentration, and bulk density of calcic horizons in the soil. (See Soil Survey Staff, 1975, p. 45–46, for a complete definition of calcic horizon.) CaCO 3 precipitates in the soil through leaching of external Ca ++ that is deposited on the surface and in the upper part of the soil, generally in the A and B horizons. The cS content, maximum stage of CaCO 3 morphology, and accumulation rate of CaCO 3 in calcic soils of equivalent age can vary over large regions of the southwestern United States in response to regional climatic patterns and the influx of Ca ++ dissolved in rainwater and solid CaCO 3 Preliminary uranium-trend ages and cS contents for relict soils of the Las Cruces, New Mexico, chronosequence show that 100,000- to 500,000-year-old soils have similar average rates of CaCO 3 accumulation. Conversely, soils formed during the past 50,000 years have accumulated CaCO 3 about twice as fast, probably because the amount of vegetative cover decreased in the Holocene and, hence, the potential supply of airborne Ca ++ and CaCO 3 to the soil surface increased. The quantitative soil-development index cS can be used to estimate the age of calcic soils. This index can also be used to correlate soils formed in unconsolidated Quaternary sediments both locally and regionally, to compare rates of secondary CaCO 3 accumulation, and to study landscape evolution as it applies to problems such as earthquake hazards and siting of critical facilities.