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• 41. [Article] Documentation of land use plan conformance and NEPA adequacy (DNA)

  Citation × Citation Citation Abstract Copy Title: Documentation of land use plan conformance and NEPA adequacy (DNA) Author: Klamath Falls Resource Area, United States. Bureau of Land Management Title: Documentation of land use plan conformance and NEPA adequacy (DNA) Author: Klamath Falls Resource Area, United States. Bureau of Land Management Close

• 42. [Article] A physical description of the Salmon River estuary

  A student report for a Civil Engineering 572 class, this document is an extensive description of the Salmon River estuary, including water flow, quality, predictions for the estuary’s future, and numerous ...

  Citation × Citation Citation Abstract Copy Title: A physical description of the Salmon River estuary Author: Noble, Scott, Higgins, Bruce, Pratt, Robert, Askren, David, Hansen, Robert A student report for a Civil Engineering 572 class, this document is an extensive description of the Salmon River estuary, including water flow, quality, predictions for the estuary’s future, and numerous charts and graphs. Title: A physical description of the Salmon River estuary Author: Noble, Scott, Higgins, Bruce, Pratt, Robert, Askren, David, Hansen, Robert A student report for a Civil Engineering 572 class, this document is an extensive description of the Salmon River estuary, including water flow, quality, predictions for the estuary’s future, and numerous charts and graphs. Close

• 43. [Image] The main business district (the "loop"), Chicago

  	Looking north, from 20th Street to beyond Randolph Street. The Chicago Drainage Canal, its source in Lake Michigan and its north and south branches are well shown. Water flows from Lake Michigan through ...
  	Citation × Citation Citation Abstract Copy Title: The main business district (the "loop"), Chicago Looking north, from 20th Street to beyond Randolph Street. The Chicago Drainage Canal, its source in Lake Michigan and its north and south branches are well shown. Water flows from Lake Michigan through the south branch of this canal into the Mississsippi River, and ultimately into the Gulf of Mexico. Title: The main business district (the "loop"), Chicago Looking north, from 20th Street to beyond Randolph Street. The Chicago Drainage Canal, its source in Lake Michigan and its north and south branches are well shown. Water flows from Lake Michigan through the south branch of this canal into the Mississsippi River, and ultimately into the Gulf of Mexico. Close

• 44. [Image] 500 ft. below great north glacier in early P.M. when water flows heavier - Cascade N. F.

  	Some of the glacial streams have dry channels in the early morning but as the ice begins to melt the stream grows until by evening it is a regular torrent. The glacier can be seen in the background.
  	Citation × Citation Citation Abstract Copy Title: 500 ft. below great north glacier in early P.M. when water flows heavier - Cascade N. F. Some of the glacial streams have dry channels in the early morning but as the ice begins to melt the stream grows until by evening it is a regular torrent. The glacier can be seen in the background. Title: 500 ft. below great north glacier in early P.M. when water flows heavier - Cascade N. F. Some of the glacial streams have dry channels in the early morning but as the ice begins to melt the stream grows until by evening it is a regular torrent. The glacier can be seen in the background. Close

• 45. [Image] Canyon near mouth of Klickitat River

  	The water flow is about 782 feet per second
  	Citation × Citation Citation Abstract Copy Title: Canyon near mouth of Klickitat River Year: 1938 The water flow is about 782 feet per second Title: Canyon near mouth of Klickitat River Year: 1938 The water flow is about 782 feet per second Close

• 46. [Article] Modeling the hydrological aspects of the Fern Lake Watershed : annual report 1971

  Data collected from the Fern Lake watershed between 1958 and 1971 include measurements of the rate of flow of water into the lake through a single inlet stream. The objective of the work presented here ...

  Citation × Citation Citation Abstract Copy Title: Modeling the hydrological aspects of the Fern Lake Watershed : annual report 1971 Author: U.S. International Biological Program. Coniferous Forest Biome, Fowler, Charles W. (Charles Winsor), 1941-, University of Washington Data collected from the Fern Lake watershed between 1958 and 1971 include measurements of the rate of flow of water into the lake through a single inlet stream. The objective of the work presented here is to develop a model of this flow using the climatological data available from the watershed. Measurements of air temperature, wind movement, air pressure, relative humidity, insolation, and precipitation were used to estimate the potential evapotranspiration through the use of the Penman equation (Penman 1948). A model based on relationships found in the published literature and some empirical relationships was developed to simulate the dynamics of the soil water. This submodel was incorporated into the larger model to link the climatological input variables to streamflow. Output from the computer program developed for the model includes soil water content, underground flow, evaporation, transpiration, and streamflow. In its tentative form, the model is sufficiently realistic to be used for further modeling of the dynamics of other aspects of the watershed involving water flow. Title: Modeling the hydrological aspects of the Fern Lake Watershed : annual report 1971 Author: U.S. International Biological Program. Coniferous Forest Biome, Fowler, Charles W. (Charles Winsor), 1941-, University of Washington Data collected from the Fern Lake watershed between 1958 and 1971 include measurements of the rate of flow of water into the lake through a single inlet stream. The objective of the work presented here is to develop a model of this flow using the climatological data available from the watershed. Measurements of air temperature, wind movement, air pressure, relative humidity, insolation, and precipitation were used to estimate the potential evapotranspiration through the use of the Penman equation (Penman 1948). A model based on relationships found in the published literature and some empirical relationships was developed to simulate the dynamics of the soil water. This submodel was incorporated into the larger model to link the climatological input variables to streamflow. Output from the computer program developed for the model includes soil water content, underground flow, evaporation, transpiration, and streamflow. In its tentative form, the model is sufficiently realistic to be used for further modeling of the dynamics of other aspects of the watershed involving water flow. Close

• 47. [Article] Water Flow through Temperate Glaciers

  Understanding water movement through a glacier is fundamental to several critical issues in glaciology, including glacier dynamics, glacier-induced floods, and the prediction of runoff from glacierized ...

  Citation × Citation Citation Abstract Copy Title: Water Flow through Temperate Glaciers Author: Fountain, Andrew G., Walder, Joseph S. Year: 1998 Understanding water movement through a glacier is fundamental to several critical issues in glaciology, including glacier dynamics, glacier-induced floods, and the prediction of runoff from glacierized drainage basins. To this end we have synthesized a conceptual model of water movement through a temperate glacier from the surface to the outlet stream. Processes that regulate the rate and distribution of water input at the glacier surface and that regulate water movement from the surface to the bed play important but commonly neglected roles in glacier hydrology. Where a glacier is covered by a layer of porous, permeable firn (the accumulation zone), the flux of water to the glacier interior varies slowly because the firn temporarily stores water and thereby smooths out variations in the supply rate. In the firn-free ablation zone, in contrast, the flux of water into the glacier depends directly on the rate of surface melt or rainfall and therefore varies greatly in time. Water moves from the surface to the bed through an upward branching arborescent network consisting of both steeply inclined conduits, formed by the enlargement of intergranular veins, and gently inclined conduits, spawned by water flow along the bottoms of near-surface fractures (crevasses). Englacial drainage conduits deliver water to the glacier bed at a limited number of points, probably a long distance downglacier of where water enters the glacier. Englacial conduits supplied from the accumulation zone are quasi steady state features that convey the slowly varying water flux delivered via the firn. Their size adjusts so that they are usually full of water and flow is pressurized. In contrast, water flow in englacial conduits supplied from the ablation area is pressurized only near times of peak daily flow or during rainstorms; flow is otherwise in an open-channel configuration. The subglacial drainage system typically consists of several elements that are distinct both morphologically and hydrologically. An upglacier branching, arborescent network of channels incised into the basal ice conveys water rapidly. Much of the water flux to the bed probably enters directly into the arborescent channel network, which covers only a small fraction of the glacier bed. More extensive spatially is a nonarborescent network, which commonly includes cavities (gaps between the glacier sole and bed), channels incised into the bed, and a layer of permeable sediment. The nonarborescent network conveys water slowly and is usually poorly connected to the arborescent system. The arborescent channel network largely collapses during winter but reforms in the spring as the first flush of meltwater to the bed destabilizes the cavities within the nonarborescent network. The volume of water stored by a glacier varies diurnally and seasonally. Small, temperate alpine glaciers seem to attain a maximum seasonal water storage of approximately 200 mm of water averaged over the area of the glacier bed, with daily fluctuations of as much as 20-30 mm. The likely storage capacity of subglacial cavities is insufficient to account for estimated stored water volumes, so most water storage may actually occur englacially. Stored water may also be released abruptly and catastrophically in the form of outburst floods. Title: Water Flow through Temperate Glaciers Author: Fountain, Andrew G., Walder, Joseph S. Year: 1998 Understanding water movement through a glacier is fundamental to several critical issues in glaciology, including glacier dynamics, glacier-induced floods, and the prediction of runoff from glacierized drainage basins. To this end we have synthesized a conceptual model of water movement through a temperate glacier from the surface to the outlet stream. Processes that regulate the rate and distribution of water input at the glacier surface and that regulate water movement from the surface to the bed play important but commonly neglected roles in glacier hydrology. Where a glacier is covered by a layer of porous, permeable firn (the accumulation zone), the flux of water to the glacier interior varies slowly because the firn temporarily stores water and thereby smooths out variations in the supply rate. In the firn-free ablation zone, in contrast, the flux of water into the glacier depends directly on the rate of surface melt or rainfall and therefore varies greatly in time. Water moves from the surface to the bed through an upward branching arborescent network consisting of both steeply inclined conduits, formed by the enlargement of intergranular veins, and gently inclined conduits, spawned by water flow along the bottoms of near-surface fractures (crevasses). Englacial drainage conduits deliver water to the glacier bed at a limited number of points, probably a long distance downglacier of where water enters the glacier. Englacial conduits supplied from the accumulation zone are quasi steady state features that convey the slowly varying water flux delivered via the firn. Their size adjusts so that they are usually full of water and flow is pressurized. In contrast, water flow in englacial conduits supplied from the ablation area is pressurized only near times of peak daily flow or during rainstorms; flow is otherwise in an open-channel configuration. The subglacial drainage system typically consists of several elements that are distinct both morphologically and hydrologically. An upglacier branching, arborescent network of channels incised into the basal ice conveys water rapidly. Much of the water flux to the bed probably enters directly into the arborescent channel network, which covers only a small fraction of the glacier bed. More extensive spatially is a nonarborescent network, which commonly includes cavities (gaps between the glacier sole and bed), channels incised into the bed, and a layer of permeable sediment. The nonarborescent network conveys water slowly and is usually poorly connected to the arborescent system. The arborescent channel network largely collapses during winter but reforms in the spring as the first flush of meltwater to the bed destabilizes the cavities within the nonarborescent network. The volume of water stored by a glacier varies diurnally and seasonally. Small, temperate alpine glaciers seem to attain a maximum seasonal water storage of approximately 200 mm of water averaged over the area of the glacier bed, with daily fluctuations of as much as 20-30 mm. The likely storage capacity of subglacial cavities is insufficient to account for estimated stored water volumes, so most water storage may actually occur englacially. Stored water may also be released abruptly and catastrophically in the form of outburst floods. Close

• 48. [Article] Sedimentologic changes in the deposits of an evolving lahar-flood in 2006, Hood River Basin, Mount Hood, Oregon

  Over a span of six days from November 2nd -- 7th, 2006 approximately 43 cm of precipitation fell over the Hood River Basin in Oregon. A lahar was initiated on the Eliot Branch of the Middle Fork Hood River ...

  Citation × Citation Citation Abstract Copy Title: Sedimentologic changes in the deposits of an evolving lahar-flood in 2006, Hood River Basin, Mount Hood, Oregon Author: Poole, Matthew Ray Year: 2016 Over a span of six days from November 2nd -- 7th, 2006 approximately 43 cm of precipitation fell over the Hood River Basin in Oregon. A lahar was initiated on the Eliot Branch of the Middle Fork Hood River by two or more landslides that occurred on the lateral moraines of the Eliot Glacier on the early part of November 7th, 2006. The Eliot Branch lahar was embedded within the larger regional flood that was occurring in the Hood River Basin and traveled a total of 48 km from the initiation points on the north flank of Mount Hood to the Hood Rivers confluence with the Columbia River. The initiating landslides abruptly transformed into a debris flow upon mixing with flood waters of the Eliot Branch. The debris flow traveled a distance of ~28 km at which point it was transformed first to a hyperconcentrated flow and then to water flow via selective deposition of coarse sediment and progressive dilution by channel flow waters from the East and West Fork Hood Rivers. The transformation from debris flow to hyperconcentrated streamflow was recorded by a thickening wedge of hyperconcentrated streamflow sediments found above and below progressively fining debris flow sediments over a reach of 22 km. Finally, the hyperconcentrated-flow phase of the lahar transformed to water flow and then traveled an additional 20 km to the Hood River delta. Upon reaching the apex of the Hood River delta, depositing sediments led to an expansion of the delta. Debris-flow sediments were predominantly gravel (36.0-69.7% by wt.) with sand (22.1-55.9% by wt.) and fines (4.7-7.8% by wt.). Hyperconcentrated flow deposits contained a larger sand fraction of (66.8-99.2% by wt.) with few gravel clasts (0-26.0% by wt.) and fines (0-8.8% by wt.). Water flow deposits averaged 90.5% (wt.) sand with 6.0% (wt.) gravel and 3.0% (wt.) fines. Sorting was a key factor in flow identification and showed progressive improvement downstream from the initiation point. Sorting values for the flow types are as follows: debris flow deposits ranged from 3.3Φ (very poorly sorted) to 1.8Φ (poorly sorted), hyperconcentrated flow deposits ranged from 2.4Φ (very poorly sorted) to 0.8Φ (moderately sorted), and water flood deposits ranged between 1.4Φ (poorly sorted) to 0.6Φ (moderately sorted). Title: Sedimentologic changes in the deposits of an evolving lahar-flood in 2006, Hood River Basin, Mount Hood, Oregon Author: Poole, Matthew Ray Year: 2016 Over a span of six days from November 2nd -- 7th, 2006 approximately 43 cm of precipitation fell over the Hood River Basin in Oregon. A lahar was initiated on the Eliot Branch of the Middle Fork Hood River by two or more landslides that occurred on the lateral moraines of the Eliot Glacier on the early part of November 7th, 2006. The Eliot Branch lahar was embedded within the larger regional flood that was occurring in the Hood River Basin and traveled a total of 48 km from the initiation points on the north flank of Mount Hood to the Hood Rivers confluence with the Columbia River. The initiating landslides abruptly transformed into a debris flow upon mixing with flood waters of the Eliot Branch. The debris flow traveled a distance of ~28 km at which point it was transformed first to a hyperconcentrated flow and then to water flow via selective deposition of coarse sediment and progressive dilution by channel flow waters from the East and West Fork Hood Rivers. The transformation from debris flow to hyperconcentrated streamflow was recorded by a thickening wedge of hyperconcentrated streamflow sediments found above and below progressively fining debris flow sediments over a reach of 22 km. Finally, the hyperconcentrated-flow phase of the lahar transformed to water flow and then traveled an additional 20 km to the Hood River delta. Upon reaching the apex of the Hood River delta, depositing sediments led to an expansion of the delta. Debris-flow sediments were predominantly gravel (36.0-69.7% by wt.) with sand (22.1-55.9% by wt.) and fines (4.7-7.8% by wt.). Hyperconcentrated flow deposits contained a larger sand fraction of (66.8-99.2% by wt.) with few gravel clasts (0-26.0% by wt.) and fines (0-8.8% by wt.). Water flow deposits averaged 90.5% (wt.) sand with 6.0% (wt.) gravel and 3.0% (wt.) fines. Sorting was a key factor in flow identification and showed progressive improvement downstream from the initiation point. Sorting values for the flow types are as follows: debris flow deposits ranged from 3.3Φ (very poorly sorted) to 1.8Φ (poorly sorted), hyperconcentrated flow deposits ranged from 2.4Φ (very poorly sorted) to 0.8Φ (moderately sorted), and water flood deposits ranged between 1.4Φ (poorly sorted) to 0.6Φ (moderately sorted). Close

• 49. [Article] Water and anion movement in selected soils of western Oregon

  Experiments were carried out to study the movement of water and halide anions in perched water tables or saturated zones in the soil and upper rock mantle of eight different experimental sites located on ...

  Citation × Citation Citation Abstract Copy Title: Water and anion movement in selected soils of western Oregon Author: Hammermeister, Dale P. Experiments were carried out to study the movement of water and halide anions in perched water tables or saturated zones in the soil and upper rock mantle of eight different experimental sites located on low hills near the western border of the Willamette Valley. At each site the experimental procedure consisted of first injecting a solution of either KBr or KI into one of three line sources located at different depths in the soil-rock mantle. Ground water samples were then periodically collected from both saturated and unsaturated depths in the soilrock mantle at points both upslope and downslope from the line source. These samples were analyzed for either I⁻ or Br⁻ by specific ion electrodes. Tensiometers and piezometers were monitored at different depths in the soil-rock mantle at each site to determine water pressure potentials (P's) which were used to calculate hydraulic gradients both in the vertical and downslope directions. Saturated hydraulic conductivity measurements were made on intact cores of soil and weathered rock from different depths at each site. In situ conductivity measurements were made where possible at depths where intact cores could not be obtained. Conductivities of intact cores were found to be log normally distributed in the A horizons, B horizons, and also possibly in the C horizons. Further, an exponential relationship was found between the percent pore space occupied by pores drained by P = -50 cm of water and the conductivity of intact cores taken from different depths at all sites. Assuming that pores drained by P = -50 cm transmit most of the water flowing through the soil-rock mantle expressions were obtained for an average pore velocity (μ) of water flowing through pores drained by P = -50 cm, and for an average pore velocity (vi) of water flowing through different pore size increments (assuming a capillary bundle model) within this pore space. Plots of P's and rainfall vs. time indicated that impermeable regions of rock near or below the 110 cm depth are mainly responsible for the development of perched water tables at most sites. Similar plots indicated that subsurface flow contributed water to sites located on lower hill slope positions. Halide anions were found to move rapidly downslope by saturated flow at all experimental sites. These rapid rates of anion movement as well as other observed characteristics of anion movement suggested that water may move through the soil-rock mantle at these sites by laminar flow through interconnected regions of high conductivity and/or via turbulent flow through macroscopic voids. To attempt to describe the maximum rates of anion movement at several sites, pore water velocity vectors μ and Vi were calculated by resolving these vectors into vertical and downslope components. μ vectors failed to account for the maximum rates of anion movement even when conductivity coefficients were selected to maximize μ in the downslope direction. However, vi vectors when maximized in the downslope direction roughly approximated the maximum rates of anion movement. This together with some additional evidence concerning the apparent or effective diffusion of halide anions in the B horizon at site 8 suggested that the capillary bundle model of the soil-rock mantle may be a good approximation of the laminar flow paths in at least several sites. However, the possibility that turbulent flow occurs through macroscopic voids in the soil-rock mantle must also be considered as a possible flow mechanism in all experimental sites. Title: Water and anion movement in selected soils of western Oregon Author: Hammermeister, Dale P. Experiments were carried out to study the movement of water and halide anions in perched water tables or saturated zones in the soil and upper rock mantle of eight different experimental sites located on low hills near the western border of the Willamette Valley. At each site the experimental procedure consisted of first injecting a solution of either KBr or KI into one of three line sources located at different depths in the soil-rock mantle. Ground water samples were then periodically collected from both saturated and unsaturated depths in the soilrock mantle at points both upslope and downslope from the line source. These samples were analyzed for either I⁻ or Br⁻ by specific ion electrodes. Tensiometers and piezometers were monitored at different depths in the soil-rock mantle at each site to determine water pressure potentials (P's) which were used to calculate hydraulic gradients both in the vertical and downslope directions. Saturated hydraulic conductivity measurements were made on intact cores of soil and weathered rock from different depths at each site. In situ conductivity measurements were made where possible at depths where intact cores could not be obtained. Conductivities of intact cores were found to be log normally distributed in the A horizons, B horizons, and also possibly in the C horizons. Further, an exponential relationship was found between the percent pore space occupied by pores drained by P = -50 cm of water and the conductivity of intact cores taken from different depths at all sites. Assuming that pores drained by P = -50 cm transmit most of the water flowing through the soil-rock mantle expressions were obtained for an average pore velocity (μ) of water flowing through pores drained by P = -50 cm, and for an average pore velocity (vi) of water flowing through different pore size increments (assuming a capillary bundle model) within this pore space. Plots of P's and rainfall vs. time indicated that impermeable regions of rock near or below the 110 cm depth are mainly responsible for the development of perched water tables at most sites. Similar plots indicated that subsurface flow contributed water to sites located on lower hill slope positions. Halide anions were found to move rapidly downslope by saturated flow at all experimental sites. These rapid rates of anion movement as well as other observed characteristics of anion movement suggested that water may move through the soil-rock mantle at these sites by laminar flow through interconnected regions of high conductivity and/or via turbulent flow through macroscopic voids. To attempt to describe the maximum rates of anion movement at several sites, pore water velocity vectors μ and Vi were calculated by resolving these vectors into vertical and downslope components. μ vectors failed to account for the maximum rates of anion movement even when conductivity coefficients were selected to maximize μ in the downslope direction. However, vi vectors when maximized in the downslope direction roughly approximated the maximum rates of anion movement. This together with some additional evidence concerning the apparent or effective diffusion of halide anions in the B horizon at site 8 suggested that the capillary bundle model of the soil-rock mantle may be a good approximation of the laminar flow paths in at least several sites. However, the possibility that turbulent flow occurs through macroscopic voids in the soil-rock mantle must also be considered as a possible flow mechanism in all experimental sites. Close

• 50. [Article] Tracing Pacific water in the North Atlantic Ocean

  copyrighted by American Geophysical Union

  Citation × Citation Citation Abstract Copy Title: Tracing Pacific water in the North Atlantic Ocean Author: McLaughlin, F. A., Civitarese, G., Jones, E. P., Kattner, G., Lipizer, M., Anderson, L. G., Falkner, Kelly, Swift, J. H. copyrighted by American Geophysical Union Title: Tracing Pacific water in the North Atlantic Ocean Author: McLaughlin, F. A., Civitarese, G., Jones, E. P., Kattner, G., Lipizer, M., Anderson, L. G., Falkner, Kelly, Swift, J. H. copyrighted by American Geophysical Union Close