Topic
Stream power
About: Stream power is a research topic. Over the lifetime, 1135 publications have been published within this topic receiving 51324 citations.
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TL;DR: In this paper, the spatial and temporal patterns of the twentieth-century channel changes of the Dunajec, the second largest river of the Polish Carpathians, are analysed using data from six historical maps, hand-auger drillings in paleochannels and hydrometric data from 10 gauging stations.
120 citations
01 Jan 2004
TL;DR: In this article, the authors distinguish diamicton facies: masses of unsorted, unstratified clays through boulders carried as a slurry during high energy flood events, (i) thalweg facies, coarse gravel to cobble size material, well winnowed, forming armoring on underground streams that moves only during flood flow, (ii) channel facies; usually well sorted and often well stratified silt though gravel carried as bedload at intermediate stream powers, (iii) slackwater facies): mostly clay and silt
Abstract: Karst aquifers demand continuous transport of clastic sediments if the conduit system is to remain open. Sediments are injected into the aquifer by sinking surface streams and through sinkholes, vertical shafts, open fractures, and other pathways from the land surface of sufficient aperture to permit gravity- and inwash-driven transport. Much transport of clastic sediments tends to be episodic with sediment loads held in storage until moved by infrequent flood events. Although the overall mix of clastic material depends on material available in the source area, distinctly different facies are recognizable depending on the flow dynamics within the conduit system. The facies are most clearly recognized when the source areas provide a wide variety of particle sizes from clays to boulders. In order of decreasing stream power, one can distinguish (i) diamicton facies: masses of unsorted, unstratified clays through boulders carried as a slurry during high energy flood events, (ii) thalweg facies: coarse gravel to cobble size material, well winnowed, forming armoring on underground streams that moves only during flood flow, (iii) channel facies: usually well sorted and often well stratified silt though gravel carried as bedload at intermediate stream powers, (iv) slackwater facies: mostly clay and silt carried as suspended load and deposited from floodwaters backfilled into the conduit system, (v) backswamp facies: mostly clay derived from the insoluble residue of the limestone, deposited under phreatic conditions with little lateral transport.
120 citations
TL;DR: In this article, a rational method has been developed to predict the regime geometry of straight active gravel streams, which is based upon a resistance equation, a bed load equation, and the condition of minimum stream power for gravel streams in equilibrium.
Abstract: A rational method has been developed to predict the regime geometry of straight active gravel streams. The analytical model is based upon a resistance equation, a bed load equation, and the condition of minimum stream power for gravel streams in equilibrium. The analytical channel geometry so obtained is in general agreement with previously established relations and observations. The analytical channel width is proportional to Q 0 . 4 7 , in which Q is the bank full discharge. Except for steep slopes, the width is essentially only a function of the discharge. The analytical depth increases with the discharge but decreases with the slope. On steep slopes, the width increases rapidly with the slope. This rapid increase in width accompanied by a decrease in depth indicates braiding tendency for steep gravel streams. As the bed load approaches zero at the lower boundary, this model for active streams reduces to the threshold theory.
120 citations
TL;DR: In this article, three types of relationship between critical specific stream power (ω 0) and grain size (D) were established, and critical values for ω 0 in the largest river (the Ourthe) were the lowest and were close to the values obtained for mountainous rivers carrying large boulders.
120 citations
TL;DR: In this paper, historical records and field data for arroyo systems of the northern Henry Mountains, south-central Utah, show that total stream power decreased in the downstream direction during a deposition period before 1896 and increased downstream during an erosion period thereafter.
Abstract: Total stream power does not necessarily increase systematically in the downstream direction because of the conflicting influences of channel slope, width, and depth. Historical records and field data for arroyo systems of the northern Henry Mountains, south-central Utah, show that total stream power decreased in the downstream direction during a deposition period before 1896 and increased downstream during an erosion period thereafter. When total stream power declined in the downstream direction, channels were small and meandering, and the ten-year flood exceeded channel capacity, resulting in overbank deposition of sediment. After an especially erosive flood in 1896, total stream power increased in the downstream direction because channels were in the bottoms of arroyos that confined discharges, resulting in channel erosion and through-put of sediment. In 1980 deposition was occurring in the headward portions of the continuous arroyo system and in the large master stream, but not in mid-basin areas. Channels in the arid and semi-arid Henry Mountains do not exhibit mutual adjustment between form and process. Rather, at times of catastrophic system-wide events, fluvial processes control channel forms, whereas at other times channel forms control fluvial processes. Comparison of historical and modern conditions shows that mutual adjustment is unlikely to occur in the discontinuous operation of semi-arid fluvial systems.
119 citations