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NARROW
GeoRef Subject
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all geography including DSDP/ODP Sites and Legs
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Africa
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Afar (1)
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Central Africa
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Congo Democratic Republic
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Kasai (1)
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East Africa
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Eritrea (1)
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North Africa
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Southern Africa
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Lesotho (1)
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Asia
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Primary terms
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Africa
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Southern Africa
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upper Pleistocene
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upper Quaternary (2)
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Tertiary
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upper Miocene
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Mount Messenger Formation (1)
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Pliocene
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upper Pliocene (1)
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Paleogene
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lower Eocene
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Invertebrata
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Insecta
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Mollusca (2)
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-
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Mesozoic
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Cretaceous
-
Bahariya Formation (1)
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Comanchean
-
Travis Peak Formation (1)
-
-
Lower Cretaceous
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Travis Peak Formation (1)
-
-
Upper Cretaceous
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Jurassic
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Navajo Sandstone (1)
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metal ores
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metals
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alkaline earth metals
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barium (1)
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mercury (2)
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mineral exploration (2)
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Piedmont (4)
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Valley and Ridge Province (3)
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-
Basin and Range Province
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Gulf Coastal Plain (1)
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oil and gas fields (2)
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oxygen
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Spermatophyta
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pool-and-riffle pattern
Paleohydrology of pool-and-riffle pattern development: Boulder Creek, Utah
Abstract This paper considers the influence of flow character upon scour and deposition loci of tracer clasts in a gravel-bed river, and discusses implications for riffle–pool maintenance. Overall, bars were found to be the dominant depositional zones where over 54% of the tracer clasts accumulated during a 13-month period, followed by riffles (31%) and, finally, pools (<15%). Variability in the location of scour and deposition zones were apparent and could be broadly linked to four flow categories: (i) low-magnitude, high-frequency flows below 29% bankfull appeared responsible for intra-unit re-distribution of sediment particles; (ii) medium-magnitude and -frequency flows (up to 70% bankfull) appeared capable of inter-unit transfer, with pool scour and immediate deposition on riffle heads downstream, and some movement from riffles to bar edges and heads; (iii) high-magnitude, low-frequency flows (70–90% bankfull) appeared capable of riffle–riffle transport, with routing around bar edges; and (iv) very high-magnitude, very low-frequency flows (bankfull and over) capable of bar to bar transport and clast transport distances exceeding the length of a single riffle–pool unit. Tracers originating from riffles do not appear to be fed into pools on the outside of meander bends, instead they appear to be routed over shallower bar surfaces. High competence and low sediment supply explains the coarse nature of the pools (D 50 =110 mm) in comparison to the riffles (D 50 = 85 mm). An improved understanding of the sediment transport mechanisms operating during different flood types is needed to better predict morphological response to changes in hydrological regime and sediment
Development of Alluvial Stream Channels: A Five-Stage Model
Medano Creek, Colorado, a model for upper-flow-regime fluvial deposition
Channel-reach morphology in mountain drainage basins
Controls on Pool Characteristics along a Resistant-Boundary Channel
ABSTRACT Wildfire frequency and intensity are increasing in many parts of the world, often with substantial repercussions for stream ecosystems. The severity, scale, and patterns of wildfire burning can differ between riparian and upland zones due to differences in environmental conditions and vegetation. However, little research has focused on differences in burn patterns in riparian versus upland zones and their implications for stream characteristics. We studied fire patterns and postfire vegetation trajectories in riparian versus upland areas across 26 stream sites in coastal southern California over 12 years, as well as the relationships of burn patterns to stream variables after fire. Upland environments burned more severely and more extensively than did riparian woodlands, and this difference was magnified for perennially flowing streams, along which riparian woodlands burned less severely than those along intermittent streams. Burned vegetation returned to prefire canopy cover and greenness in both riparian and upland areas in about 8 years with regrowth delayed by a prolonged drought. Additionally, we observed differences in spatial burn patterns and vegetation regrowth in upland versus riparian zones, with greater local patchiness in upland settings, likely due to differences between upland and riparian areas in the spatial patterns of hydrologic, topographic, and vegetative drivers of fire and vegetation reestablishment. We then assessed relationships between spatial fire patterns and geomorphological, physical, hydrochemical, and biological conditions at creek sites. We observed relationships that were generally attributable to either the local destruction of riparian woodland along the streams or to changes in the basin-scale movement of water, nutrients, and sediment following fire and postfire floods. Basin-scale burn patterns were associated with increases in sediment deposition, reduction in pool and riffle habitat extents, and changes in particulate organic matter during the first and second years after fires; impacts subsided about a year after the first substantial postfire flows. In contrast, loss of riparian canopy cover was associated with increases in light level, temperature, algal cover and biomass, density of algivorous invertebrates and amphibians, and water conductivity, as well as decreases in particulate organic matter and invertebrate shredders. In contrast to impacts from basin-scale burn patterns, impacts from the local loss of riparian canopy cover persisted for longer periods of time, paralleling riparian woodland reestablishment and growth.
Variables influencing water-surface slopes in gravel-bed streams at bankfull stage
Techniques and interpretation: The sediment studies of G. K. Gilbert
The laboratory experiments on sediment transport conducted by G. K. Gilbert differed importantly in technique from such studies of more recent date. Gilbert’s flume was level and could not be altered in slope. Sediment was introduced at the upper end at a predetermined rate and by deposition built a bed gradient sufficient to transport the introduced load. The adjustment of slope in Gilbert’s flume has contributed to the idea widely held by geologists that a river achieves equilibrium by adjusting its slope to provide just the velocity required for the transportation of the supplied load. In fact, slope adjusts but little to a change in amount of introduced sediment load. The adjustment takes place principally among other hydraulic factors: width, depth, velocity, bed forms, channel pattern, and pool-riffle sequence. Gilbert sensed this complicated adjustment process, but its details are as yet only partially known in quantitative terms.