The 13 major south-shore streams in Nassau and Suffolk Counties, Long Island, New York with adequate long-term (1971-97) water-quality records, and 192 south-shore wells with sufficient water-quality data, were selected for analysis of geographic, seasonal, and long-term trends in nitrogen concentration. Annual total nitrogen loads transported to the South Shore Estuary Reserve (SSER) from 11 of these streams were calculated using long-term discharge records. Nitrogen loads from shallow and deep ground water also were calculated using simulated ground-water discharge of 1968-83 hydrologic conditions.
Long-term declines in stream discharge occurred in East Meadow Brook, Bellmore Creek and Massapequa Creek in response to extensive sewering in Nassau County. The smallest longterm annual discharge to the SSER was from the westernmost stream, Pines Brook, which is in an area in which the water table has been lowered by sewers since 1952. The three largest average annual discharges to the SSER were from the Connetquot River, Carlls River, and Carmans River in Suffolk County; the discharges from each of these streams were at least twice those of the other streams considered in this study.
Total nitrogen concentrations in streams show a geographic trend with a general eastward increase in median total nitrogen concentration in Nassau County and a decreasing trend from Massapequa Creek eastward into Suffolk County. Total nitrogen concentrations in streams generally are lowest during summer and highest in winter as a result of seasonal fluctuations in chemical reactions and biological activity. The greatest seasonal difference in median total nitrogen concentration was at Carlls River with values of 3.4 and 4.2 mg/L (milligrams per liter) as N during summer (April through September) and winter (October through March), respectively. Streams affected by the completion of sewer districts show long-term (1971-97) trends of decreasing total nitrogen concentration and streams showing an increase in total nitrogen concentration are in unsewered areas with increased urbanization.
Discharges from shallow ground water (upper glacial aquifer) and deep ground water (upper part of Magothy aquifer) were simulated from a ground-water-flow model calibrated to steadystate (1968-83) conditions. Simulated discharges from shallow-ground-water system in Nassau County were 10,700 Mgal/yr (million gallons per year) or 40,500,000 m3/yr (cubic meters per year), and those from Suffolk County were 52,300 Mgal/yr or 198,000,000 m3/yr. Discharges from deep-ground-water system in Nassau County were 4,900 Mgal/yr or 18,500,000 m3/yr, and those in Suffolk County were 12,700 Mgal/yr or 48,200,000 m3/yr.
Ground-water concentrations of nitrogen decrease with depth and from west to east. The shallow ground water median nitrogen concentration for each county was determined using 1,155 samples collected at 167 shallow wells (125 feet deep or less) within 1 mile of the shore. The deep ground water median nitrate concentration (nitrate represented almost all of the total nitrogen) for each county was determined using 112 samples collected at 25 deep wells (greater than 125 feet deep) within 1 mile of the shore. The median nitrogen concentration for the shallow and median nitrate concentration for the deep ground water in Nassau County were 3.85 and 0.15 mg/L as N, during 1952–97; the corresponding concentrations for Suffolk County were 1.74 and <0.10 (less than 0.10) mg/L as N, during 1952–97.
Nitrogen loads discharged from streams to the SSER for each year during 1972–97 were calculated as the annual total nitrogen concentration multiplied by the annual discharge. These values were calculated only for the seven streams for which sufficient data were available. The largest long-term (1972–97) average annual nitrogen load from Carlls River was 104 ton/yr or 94,300 kg/yr—about twice that of Connetquot River (54 ton/yr or 48,900 kg/yr) and over three times that of Carmans River (33 ton/yr or 29,900 kg/yr). The smallest annual mean nitrogen load was from Pines Brook, which has the lowest annual mean discharge of all streams analyzed.
The nitrogen load carried to the SSER by ground-water discharge in shallow-ground-water system in Nassau and Suffolk Counties was calculated as the simulated discharge for each county multiplied by the respective median nitrogen concentration, and loads from deep-ground-water system were calculated as the simulated discharge for each county multiplied by the respective median nitrate concentration. All discharges were obtained from the U.S. Geological Survey's Long Island ground-water-flow model. The resultant nitrogen loads discharged to the SSER from shallow ground water were 172 ton/yr (156,000 kg/yr) from Nassau County and 380 ton/yr (345,000 kg/yr) from Suffolk County; equaling 552 ton/yr entering the SSER. Those from deep ground water were 3 ton/yr (2,700 kg/yr) from Nassau County and <0.5 ton/yr (480 kg/yr) from Suffolk County; equaling about 3.5 ton/yr entering the SSER.
The sum of both stream loads and groundwater loads results in the total load to the SSER. The largest calculated total nitrogen load entering the SSER from both streams and ground water occurred in 1979 with a total load of 1,260 ton/yr (1,140,000 kg/yr). The smallest calculated nitrogen load entering the SSER occurred in 1995 with a total load of 725 ton/yr (658,000 kg/yr).
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024255","collaboration":"Prepared in cooperation with the New York State Department of State","usgsCitation":"Monti, and Scorca, M.P., 2003, Trends in nitrogen concentration and nitrogen loads entering the South Shore Estuary Reserve from streams and ground-water discharge in Nassau and Suffolk counties, Long Island, New York, 1952–97: U.S. Geological Survey Water-Resources Investigations Report 2002-4255, v, 36 p., https://doi.org/10.3133/wri024255.","productDescription":"v, 36 p.","onlineOnly":"N","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":411008,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54607.htm","linkFileType":{"id":5,"text":"html"}},{"id":3694,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4255/wri20024255.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2002-4255"},{"id":168541,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4255/coverthb.jpg"}],"country":"United States","state":"New York","county":"Nassau County, Suffolk County","otherGeospatial":"Long Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -72.5,\n 41.875\n ],\n [\n -73.7625,\n 41.875\n ],\n [\n -73.7625,\n 40.5861\n ],\n [\n -72.5,\n 40.5861\n ],\n [\n -72.5,\n 41.875\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","contact":"Director, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
The data files and explanations presented in this report were used to generate published material-balance approach estimates of amounts of petroleum 1) expelled from a source rock, and the sum of 2) petroleum discovered in-place plus that lost due to 3) secondary migration within, or leakage or erosion from a petroleum system. This study includes assessment of cumulative production, known petroleum volume, and original oil in place for hydrocarbons that were generated from the New Albany Shale source rocks. More than 4.00 billion barrels of oil (BBO) have been produced from Pennsylvanian-, Mississippian-, Devonian-, and Silurian-age reservoirs in the New Albany Shale petroleum system. Known petroleum volume is 4.16 BBO; the average recovery factor is 103.9% of the current cumulative production. Known petroleum volume of oil is 36.22% of the total original oil in place of 11.45 BBO. More than 140.4 BBO have been generated from the Upper Devonian and Lower Mississippian New Albany Shale in the Illinois Basin. Approximately 86.29 billion barrels of oil that was trapped south of the Cottage Grove fault system were lost by erosion of reservoir intervals. The remaining 54.15 BBO are 21% of the hydrocarbons that were generated in the basin and are accounted for using production data. Included in this publication are 2D maps that show the distribution of production for different formations versus the Rock-Eval pyrolysis hydrogen-indices (HI) contours, and 3D images that show the close association between burial depth and HI values.The primary vertical migration pathway of oil and gas was through faults and fractures into overlying reservoir strata. About 66% of the produced oil is located within the generative basin, which is outlined by an HI contour of 400. The remaining production is concentrated within 30 miles (50 km) outside the 400 HI contour. The generative basin is subdivided by contours of progressively lower hydrogen indices that represent increased levels of thermal maturity and generative capacity of New Albany Shale source rocks. The generative basin was also divided into seven oil-migration catchments. The catchments were determined using a surface-flow hydrologic model with contoured HI values as input to the model.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr200337","usgsCitation":"Higley, D.K., Henry, M.E., Lewan, M.D., and Pitman, J.K., 2003, The New Albany Shale petroleum system, Illinois basin - Data and map image archive from the material-balance assessment (Supersedes Open-File Report 01-162): U.S. Geological Survey Open-File Report 2003-37, HTML Document, https://doi.org/10.3133/ofr200337.","productDescription":"HTML Document","onlineOnly":"Y","costCenters":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":178241,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":402720,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54654.htm","linkFileType":{"id":5,"text":"html"}},{"id":4596,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2003/ofr-03-037/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Illinois, Indiana","otherGeospatial":"Illinois basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -89.219970703125,\n 37.75334401310656\n ],\n [\n -86.11083984375,\n 37.75334401310656\n ],\n [\n -86.11083984375,\n 40.84706035607122\n ],\n [\n -89.219970703125,\n 40.84706035607122\n ],\n [\n -89.219970703125,\n 37.75334401310656\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Supersedes Open-File Report 01-162","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac7e4b07f02db67ad4d","contributors":{"authors":[{"text":"Higley, Debra K. 0000-0001-8024-9954 higley@usgs.gov","orcid":"https://orcid.org/0000-0001-8024-9954","contributorId":152663,"corporation":false,"usgs":true,"family":"Higley","given":"Debra","email":"higley@usgs.gov","middleInitial":"K.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":242349,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Henry, M. E.","contributorId":103734,"corporation":false,"usgs":true,"family":"Henry","given":"M.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":242352,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lewan, M. D.","contributorId":46540,"corporation":false,"usgs":true,"family":"Lewan","given":"M.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":242350,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Pitman, Janet K. 0000-0002-0441-779X jpitman@usgs.gov","orcid":"https://orcid.org/0000-0002-0441-779X","contributorId":767,"corporation":false,"usgs":true,"family":"Pitman","given":"Janet","email":"jpitman@usgs.gov","middleInitial":"K.","affiliations":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true},{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":242351,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":47779,"text":"wri034016 - 2003 - Simulation of ground-water flow and land subsidence in the Antelope Valley ground-water basin, California","interactions":[],"lastModifiedDate":"2012-02-02T00:10:41","indexId":"wri034016","displayToPublicDate":"2003-05-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2003-4016","title":"Simulation of ground-water flow and land subsidence in the Antelope Valley ground-water basin, California","docAbstract":"Antelope Valley, California, is a topographically closed basin in the western part of the Mojave Desert, about 50 miles northeast of Los Angeles. The Antelope Valley ground-water basin is about 940 square miles and is separated from the northern part of Antelope Valley by faults and low-lying hills. Prior to 1972, ground water provided more than 90 percent of the total water supply in the valley; since 1972, it has provided between 50 and 90 percent. Most ground-water pumping in the valley occurs in the Antelope Valley ground-water basin, which includes the rapidly growing cities of Lancaster and Palmdale. Ground-water-level declines of more than 200 feet in some parts of the ground-water basin have resulted in an increase in pumping lifts, reduced well efficiency, and land subsidence of more than 6 feet in some areas. Future urban growth and limits on the supply of imported water may continue to increase reliance on ground water. To better understand the ground-water flow system and to develop a tool to aid in effectively managing the water resources, a numerical model of ground-water flow and land subsidence in the Antelope Valley ground-water basin was developed using old and new geohydrologic information.\r\n\r\n\r\nThe ground-water flow system consists of three aquifers: the upper, middle, and lower aquifers. The aquifers, which were identified on the basis of the hydrologic properties, age, and depth of the unconsolidated deposits, consist of gravel, sand, silt, and clay alluvial deposits and clay and silty clay lacustrine deposits. Prior to ground-water development in the valley, recharge was primarily the infiltration of runoff from the surrounding mountains. Ground water flowed from the recharge areas to discharge areas around the playas where it discharged either from the aquifer system as evapotranspiration or from springs. Partial barriers to horizontal ground-water flow, such as faults, have been identified in the ground-water basin. Water-level declines owing to ground-water development have eliminated the natural sources of discharge, and pumping for agricultural and urban uses have become the primary source of discharge from the ground-water system. Infiltration of return flows from agricultural irrigation has become an important source of recharge to the aquifer system.\r\n\r\n\r\nThe ground-water flow model of the basin was discretized horizontally into a grid of 43 rows and 60 columns of square cells 1 mile on a side, and vertically into three layers representing the upper, middle, and lower aquifers. Faults that were thought to act as horizontal-flow barriers were simulated in the model. The model was calibrated to simulate steady-state conditions, represented by 1915 water levels and transient-state conditions during 1915-95 using water-level and subsidence data. Initial estimates of the aquifer-system properties and stresses were obtained from a previously published numerical model of the Antelope Valley ground-water basin; estimates also were obtained from recently collected hydrologic data and from results of simulations of ground-water flow and land subsidence models of the Edwards Air Force Base area. Some of these initial estimates were modified during model calibration. Ground-water pumpage for agriculture was estimated on the basis of irrigated crop acreage and crop consumptive-use data. Pumpage for public supply, which is metered, was compiled and entered into a database used for this study. Estimated annual pumpage peaked at 395,000 acre-feet (acre-ft) in 1952 and then declined because of declining agricultural production. Recharge from irrigation-return flows was estimated to be 30 percent of agricultural pumpage; the irrigation-return flows were simulated as recharge to the regional water table 10 years following application at land surface. The annual quantity of natural recharge initially was based on estimates from previous studies. During model calibration, natural recharge was reduced from the initial","language":"ENGLISH","doi":"10.3133/wri034016","usgsCitation":"Leighton, D.A., and Phillips, S.P., 2003, Simulation of ground-water flow and land subsidence in the Antelope Valley ground-water basin, California: U.S. Geological Survey Water-Resources Investigations Report 2003-4016, 118 p., https://doi.org/10.3133/wri034016.","productDescription":"118 p.","costCenters":[],"links":[{"id":3991,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri034016","linkFileType":{"id":5,"text":"html"}},{"id":171789,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b06e4b07f02db69a20d","contributors":{"authors":[{"text":"Leighton, David A.","contributorId":95493,"corporation":false,"usgs":true,"family":"Leighton","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":236218,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Phillips, Steven P. 0000-0002-5107-868X sphillip@usgs.gov","orcid":"https://orcid.org/0000-0002-5107-868X","contributorId":1506,"corporation":false,"usgs":true,"family":"Phillips","given":"Steven","email":"sphillip@usgs.gov","middleInitial":"P.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236217,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":47791,"text":"wri034023 - 2003 - A stream-gaging network analysis for the 7-day, 10-year annual low flow in New Hampshire streams","interactions":[],"lastModifiedDate":"2017-07-27T13:28:39","indexId":"wri034023","displayToPublicDate":"2003-05-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2003-4023","title":"A stream-gaging network analysis for the 7-day, 10-year annual low flow in New Hampshire streams","docAbstract":"The 7-day, 10-year (7Q10) low-flow-frequency statistic is a widely used measure of surface-water availability in New Hampshire. Regression equations and basin-characteristic digital data sets were developed to help water-resource managers determine surface-water resources during periods of low flow in New Hampshire streams. These regression equations and data sets were developed to estimate streamflow statistics for the annual and seasonal low-flow-frequency, and period-of-record and seasonal period-of-record flow durations. generalized-least-squares (GLS) regression methods were used to develop the annual 7Q10 low-flow-frequency regression equation from 60 continuous-record stream-gaging stations in New Hampshire and in neighboring States. In the regression equation, the dependent variables were the annual 7Q10 flows at the 60 stream-gaging stations. The independent (or predictor) variables were objectively selected characteristics of the drainage basins that contribute flow to those stations. In contrast to ordinary-least-squares (OLS) regression analysis, GLS-developed estimating equations account for differences in length of record and spatial correlations among the flow-frequency statistics at the various stations.
A total of 93 measurable drainage-basin characteristics were candidate independent variables. On the basis of several statistical parameters that were used to evaluate which combination of basin characteristics contribute the most to the predictive power of the equations, three drainage-basin characteristics were determined to be statistically significant predictors of the annual 7Q10: (1) total drainage area, (2) mean summer stream-gaging station precipitation from 1961 to 90, and (3) average mean annual basinwide temperature from 1961 to 1990.
To evaluate the effectiveness of the stream-gaging network in providing regional streamflow data for the annual 7Q10, the computer program GLSNET (generalized-least-squares NETwork) was used to analyze the network by application of GLS regression between streamflow and the climatic and basin characteristics of the drainage basin upstream from each stream-gaging station. Improvement to the predictive ability of the regression equations developed for the network analyses is measured by the reduction in the average sampling-error variance, and can be achieved by collecting additional streamflow data at existing stations. The predictive ability of the regression equations is enhanced even further with the addition of new stations to the network. Continued data collection at unregulated stream-gaging stations with less than 14 years of record resulted in the greatest cost-weighted reduction to the average sampling-error variance of the annual 7Q10 regional regression equation. The addition of new stations in basins with underrepresented values for the independent variables of the total drainage area, average mean annual basinwide temperature, or mean summer stream-gaging station precipitation in the annual 7Q10 regression equation yielded a much greater cost-weighted reduction to the average sampling-error variance than when more data were collected at existing unregulated stations. To maximize the regional information obtained from the stream-gaging network for the annual 7Q10, ranking of the streamflow data can be used to determine whether an active station should be continued or if a new or discontinued station should be activated for streamflow data collection. Thus, this network analysis can help determine the costs and benefits of continuing the operation of a particular station or activating a new station at another location to predict the 7Q10 at ungaged stream reaches. The decision to discontinue an existing station or activate a new station, however, must also consider its contribution to other water-resource analyses such as flood management, water quality, or trends in land use or climatic change.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri034023","collaboration":"Prepared in cooperation with the New Hampshire Department of Environmental Services","usgsCitation":"Flynn, R.H., 2003, A stream-gaging network analysis for the 7-day, 10-year annual low flow in New Hampshire streams: U.S. Geological Survey Water-Resources Investigations Report 2003-4023, 39 p., https://doi.org/10.3133/wri034023.","productDescription":"39 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"links":[{"id":171039,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2003/4023/coverthb.jpg"},{"id":344328,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2003/4023/wri20034023.pdf","text":"Report","size":"1.80 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2003-4023"}],"contact":"Director, New England Water Science Center
U.S. Geological Survey
361 Commerce Way
Pembroke, NH 03275
The neighboring cities of El Paso, Texas, and Ciudad Juarez, Chihuahua, Mexico, have historically relied on ground-water withdrawals from the Hueco Bolson, an alluvial-aquifer system, to supply water to their growing populations. By 1996, ground-water drawdown exceeded 60 meters in some areas under Ciudad Juarez and El Paso.
A simulation of steady-state and transient ground-water flow in the Hueco Bolson in westernmost Texas, south-central New Mexico, and northern Chihuahua, Mexico, was developed using MODFLOW-96. The model is needed by El Paso Water Utilities to evaluate strategies for obtaining the most beneficial use of the Hueco Bolson aquifer system. The transient simulation represents a period of 100 years beginning in 1903 and ending in 2002. The period 1903 through 1968 was represented with 66 annual stress periods, and the period 1969 through 2002 was represented with 408 monthly stress periods.
The ground-water flow model was calibrated using MODFLOWP and UCODE. Parameter values representing aquifer properties and boundary conditions were adjusted through nonlinear regression in a transient-state simulation with 96 annual time steps to produce a model that approximated (1) 4,352 water levels measured in 292 wells from 1912 to 1995, (2) three seepage-loss rates from a reach of the Rio Grande during periods from 1979 to 1981, (3) three seepage-loss rates from a reach of the Franklin Canal during periods from 1990 to 1992, and (4) 24 seepage rates into irrigation drains from 1961 to 1983. Once a calibrated model was obtained with MODFLOWP and UCODE, the optimal parameter set was used to create an equivalent MODFLOW-96 simulation with monthly temporal discretization to improve computations of seepage from the Rio Grande and to define the flow field for a chloride-transport simulation.
Model boundary conditions were modified at appropriate times during the simulation to represent changes in well pumpage, drainage of agricultural fields, and channel modifications of the Rio Grande. The model input was generated from geographic information system databases, which facilitated rapid model construction and enabled testing of several conceptualizations of hydrogeologic facies boundaries. Specific yield of unconfined layers and hydraulic conductance of Quaternary faults in the fluvial facies were the most sensitive model parameters, suggesting that ground-water flow is impeded across the fault planes.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024108","collaboration":"Prepared in cooperation with El Paso Water Utilities and the U.S. Army–Fort Bliss","usgsCitation":"Heywood, C.E., and Yager, R.M., 2003, Simulated ground-water flow in the Hueco Bolson, an alluvial-basin aquifer system near El Paso, Texas: U.S. Geological Survey Water-Resources Investigations Report 2002-4108, v, 73 p., https://doi.org/10.3133/wri024108.","productDescription":"v, 73 p.","numberOfPages":"80","costCenters":[{"id":472,"text":"New Mexico Water Science Center","active":true,"usgs":true}],"links":[{"id":4079,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4108/wrir024108.pdf","text":"Report","size":"5.35 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRIR 2002–4108"},{"id":359968,"rank":2,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4108/coverthb.jpg"}],"contact":"Director, New Mexico Water Science Center
U.S. Geological Survey
6700 Edith Blvd NE
Albuquerque, NM 87113
Water-quality samples were collected at 10 sites in the Clark Fork-Pend Oreille and Spokane River Basins in water years 1999 – 2001 as part of the Northern Rockies Intermontane Basins (NROK) National Water-Quality Assessment (NAWQA) Program. Sampling sites were located in varied environments ranging from small streams and rivers in forested, mountainous headwater areas to large rivers draining diverse landscapes. Two sampling sites were located immediately downstream from the large lakes; five sites were located downstream from large-scale historical mining and oreprocessing areas, which are now the two largest “Superfund” (environmental remediation) sites in the Nation. Samples were collected during a wide range of streamflow conditions, more frequently during increasing and high streamflow and less frequently during receding and base-flow conditions. Sample analyses emphasized major ions, nutrients, and selected trace elements.
\nStreamflow during the study ranged from more than 130 percent of the long-term average in 1999 at some sites to 40 percent of the long-term average in 2001. River and stream water in the study area exhibited small values for specific conductance, hardness, alkalinity, and dissolved solids. Dissolved oxygen concentrations in almost all samples were near saturation. Median total nitrogen and total phosphorus concentrations in samples from most sites were smaller than median concentrations reported for many national programs and other NAWQA Program study areas. The only exceptions were two sites downstream from large wastewater-treatment facilities, where median concentrations of total nitrogen exceeded the national median. Maximum concentrations of total phosphorus in samples from six sites exceeded the 0.1 milligram per liter threshold recommended for limiting nuisance aquatic growth. Concentrations of arsenic, cadmium, copper, lead, mercury, and zinc were largest in samples from sites downstream from historical mining and ore-processing areas in the upper Clark Fork in Montana and the South Fork Coeur d’Alene River in Idaho. Concentrations of dissolved lead in all 32 samples from the South Fork Coeur d’Alene River exceeded the Idaho chronic criterion for the protection of aquatic life at the median hardness level measured during the study. Concentrations of dissolved zinc in all samples collected at this site exceeded both the chronic and acute criteria at all hardness levels measured.
\nWhen all data from all NROK sites were combined, median concentrations of dissolved arsenic, dissolved and total recoverable copper, total recoverable lead, and total recoverable zinc in the NROK study area appeared to be similar to or slightly smaller than median concentrations at sites in other NAWQA Program study areas in the Western United States affected by historical mining activities. Although the NROK median total recoverable lead concentration was the smallest among the three Western study areas compared, concentrations in several NROK samples were an order of magnitude larger than the maximum concentrations measured in the Upper Colorado River and Great Salt Lake Basins. Dissolved cadmium, dissolved lead, and total recoverable zinc concentrations at NROK sites were more variable than in the other study areas; concentrations ranged over almost three orders of magnitude between minimum and maximum values; the range of dissolved zinc concentrations in the NROK study area exceeded three orders of magnitude.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr02472","usgsCitation":"Beckwith, M.A., 2003, Summary of surface-water-quality data collected for the Northern Rockies Intermontane Basins National Water-Quality Assessment Program in the Clark Fork-Pend Oreille and Spokane River basins, Montana, Idaho, and Washington, water years 1999-2001: U.S. Geological Survey Open-File Report 2002-472, viii, 47 p., https://doi.org/10.3133/ofr02472.","productDescription":"viii, 47 p.","numberOfPages":"56","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":262370,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2002/0472/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":407871,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54625.htm","linkFileType":{"id":5,"text":"html"}},{"id":262371,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2002/0472/report-thumb.jpg"}],"country":"United States","state":"Idaho, Montana, Washington","otherGeospatial":"Clark Fork-Pend Oreille and Spokane River basins","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.3444,\n 45.4667\n ],\n [\n -112.2,\n 45.4667\n ],\n [\n -112.2,\n 49\n ],\n [\n -118.3444,\n 49\n ],\n [\n -118.3444,\n 45.4667\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b01e4b07f02db69893b","contributors":{"authors":[{"text":"Beckwith, Michael A.","contributorId":66670,"corporation":false,"usgs":true,"family":"Beckwith","given":"Michael","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":241883,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":44929,"text":"wri024264 - 2003 - Simulation of Ground-Water Flow in the Irwin Basin Aquifer System, Fort Irwin National Training Center, California","interactions":[],"lastModifiedDate":"2012-02-02T00:04:57","indexId":"wri024264","displayToPublicDate":"2003-04-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4264","title":"Simulation of Ground-Water Flow in the Irwin Basin Aquifer System, Fort Irwin National Training Center, California","docAbstract":"Ground-water pumping in the Irwin Basin at Fort Irwin National Training Center, California resulted in water-level declines of about 30 feet from 1941 to 1996. Since 1992, artificial recharge from wastewater-effluent infiltration and irrigation-return flow has stabilized water levels, but there is concern that future water demands associated with expansion of the base may cause a resumption of water-level declines. To address these concerns, a ground-water flow model of the Irwin Basin was developed to help better understand the aquifer system, assess the long-term availability and quality of ground water, and evaluate ground-water conditions owing to current pumping and to plan for future water needs at the base. \r\n\r\n\r\n\r\nHistorical data show that ground-water-level declines in the Irwin Basin between 1941 and 1996, caused the formation of a pumping depression near the pumped wells, and that recharge from the wastewater-treatment facility and disposal area caused the formation of a recharge mound. There have been two periods of water-level recovery in the Irwin Basin since the development of ground water in this basin; these periods coincide with a period of decreased pumpage from the basin and a period of increased recharge of water imported from the Bicycle Basin beginning in 1967 and from the Langford Basin beginning in 1992. Since 1992, artificial recharge has exceeded pumpage in the Irwin Basin and has stabilized water-level declines. \r\n\r\n\r\n\r\nA two-layer ground-water flow model was developed to help better understand the aquifer system, assess the long-term availability and quality of ground water, and evaluate ground-water conditions owing to current pumping and to plan for future water needs at the base. Boundary conditions, hydraulic conductivity, altitude of the bottom of the layers, vertical conductance, storage coefficient, recharge, and discharge were determined using existing geohydrologic data. Rates and distribution of recharge and discharge were determined from existing data and estimated when unavailable. \r\n\r\n\r\n\r\nResults of predictive simulations indicate that in 50 years, if artificial recharge continues to exceed pumpage in Irwin Basin, water levels could rise as much as 65 feet beneath the pumping depression, and as much as 10 feet in the wastewater-treatment facility and disposal area. \r\n\r\n\r\nParticle-tracking simulations were used to determine the pathlines and the traveltimes of water high in dissolved solids into the main pumping area. The pathlines of particles from two areas with high dissolved-solids concentrations show that in 50 years water from these areas almost reaches the nearest pumped well.","language":"ENGLISH","doi":"10.3133/wri024264","usgsCitation":"Densmore, J., 2003, Simulation of Ground-Water Flow in the Irwin Basin Aquifer System, Fort Irwin National Training Center, California: U.S. Geological Survey Water-Resources Investigations Report 2002-4264, 69 p., https://doi.org/10.3133/wri024264.","productDescription":"69 p.","costCenters":[],"links":[{"id":3805,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri024264","linkFileType":{"id":5,"text":"html"}},{"id":134887,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699f1b","contributors":{"authors":[{"text":"Densmore, Jill N. 0000-0002-5345-6613","orcid":"https://orcid.org/0000-0002-5345-6613","contributorId":89179,"corporation":false,"usgs":true,"family":"Densmore","given":"Jill N.","affiliations":[],"preferred":false,"id":230706,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":51484,"text":"ofr0350 - 2003 - Map showing alpine debris flows triggered by a July 28, 1999 thunderstorm in the central Front Range of Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:11:34","indexId":"ofr0350","displayToPublicDate":"2003-03-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2003-50","title":"Map showing alpine debris flows triggered by a July 28, 1999 thunderstorm in the central Front Range of Colorado","docAbstract":"This 1:24,000-scale map shows an inventory of debris flows that were triggered above timberline by a thunderstorm in the central Front Range of Colorado. We have classified the debris flows into two categories based on the style of initiation processes in the debris-flow source areas: 1) soil slip, and 2) non-soil slip erosive processes. This map and associated digital data are part of a larger study of the debris-flow event, results of which we plan to present in a forthcoming paper.","language":"ENGLISH","doi":"10.3133/ofr0350","usgsCitation":"Godt, J.W., and Coe, J.A., 2003, Map showing alpine debris flows triggered by a July 28, 1999 thunderstorm in the central Front Range of Colorado (Version 1.0): U.S. Geological Survey Open-File Report 2003-50, map and text (4 p.), https://doi.org/10.3133/ofr0350.","productDescription":"map and text (4 p.)","costCenters":[],"links":[{"id":110392,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54494.htm","linkFileType":{"id":5,"text":"html"},"description":"54494"},{"id":176999,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":4485,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2003/ofr-03-050/","linkFileType":{"id":5,"text":"html"}}],"edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a94e4b07f02db658e5e","contributors":{"authors":[{"text":"Godt, Jonathan W. 0000-0002-8737-2493 jgodt@usgs.gov","orcid":"https://orcid.org/0000-0002-8737-2493","contributorId":1166,"corporation":false,"usgs":true,"family":"Godt","given":"Jonathan","email":"jgodt@usgs.gov","middleInitial":"W.","affiliations":[{"id":508,"text":"Office of the AD Hazards","active":true,"usgs":true},{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true}],"preferred":true,"id":243711,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Coe, Jeffrey A. 0000-0002-0842-9608 jcoe@usgs.gov","orcid":"https://orcid.org/0000-0002-0842-9608","contributorId":1333,"corporation":false,"usgs":true,"family":"Coe","given":"Jeffrey","email":"jcoe@usgs.gov","middleInitial":"A.","affiliations":[{"id":309,"text":"Geology and Geophysics Science Center","active":true,"usgs":true},{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true}],"preferred":true,"id":243712,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":51511,"text":"ofr036 - 2003 - Principal facts for gravity stations in the Dry Valley area, west-central Nevada and east-central California","interactions":[],"lastModifiedDate":"2023-06-23T15:09:26.510101","indexId":"ofr036","displayToPublicDate":"2003-03-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2003-6","title":"Principal facts for gravity stations in the Dry Valley area, west-central Nevada and east-central California","docAbstract":"In June, 2002, the U.S. Geological Survey (USGS) established 143 new gravity stations and 12 new rock samples in the Dry Valley area, 30 miles north of Reno, Nevada, on the California - Nevada border (see fig. 1). This study reports on gravity, magnetic, and physical property data intended for use in modeling the geometry and depth of Dry Valley for groundwater analysis. It is part of a larger study that aims to characterize the hydrologic framework of several basins in Washoe County. Dry Valley is located south of the Fort Sage Mountains and south-east of Long Valley, on USGS 7.5’ quadrangles Constantia and Seven Lakes (fig. 2). The Cretaceous granitic rocks and Tertiary volcanic rocks that bound the sediment filled basin (fig. 3) may be especially important to future modeling because of their impact on groundwater flow. The granitic and volcanic rocks of Dry Valley exhibit densities and magnetic susceptibilities higher than the overlaying sediments, and create a distinguishable pattern of gravity and magnetic anomalies that reflect these properties.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr036","usgsCitation":"Sanger, E.A., and Ponce, D.A., 2003, Principal facts for gravity stations in the Dry Valley area, west-central Nevada and east-central California: U.S. Geological Survey Open-File Report 2003-6, Report: 21 p.; 7 Plates: 8.50 x 11.00 inches, https://doi.org/10.3133/ofr036.","productDescription":"Report: 21 p.; 7 Plates: 8.50 x 11.00 inches","onlineOnly":"Y","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":285218,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/7_pro.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"}},{"id":285217,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/6_pro.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"}},{"id":285216,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/5_mag.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"}},{"id":285215,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/4_iso.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"}},{"id":285214,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/3_geol.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"}},{"id":285213,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/2_topo.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"}},{"id":285212,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/1_index.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"}},{"id":285211,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2003/0006/pdf/of03-6.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}},{"id":178555,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr036.jpg"},{"id":4518,"rank":10,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2003/0006/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"California, Nevada","otherGeospatial":"Dry Valley area","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -120.25,39.875 ], [ -120.25,40.125 ], [ -119.75,40.125 ], [ -119.75,39.875 ], [ -120.25,39.875 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db667e1a","contributors":{"authors":[{"text":"Sanger, Elizabeth A.","contributorId":50219,"corporation":false,"usgs":true,"family":"Sanger","given":"Elizabeth","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":243778,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ponce, David A. 0000-0003-4785-7354 ponce@usgs.gov","orcid":"https://orcid.org/0000-0003-4785-7354","contributorId":1049,"corporation":false,"usgs":true,"family":"Ponce","given":"David","email":"ponce@usgs.gov","middleInitial":"A.","affiliations":[{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true},{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":243777,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":50867,"text":"ofr0317 - 2003 - Preliminary soil-slip susceptibility maps, southwestern California","interactions":[],"lastModifiedDate":"2023-06-23T15:17:41.159722","indexId":"ofr0317","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2003-17","title":"Preliminary soil-slip susceptibility maps, southwestern California","docAbstract":"This group of maps shows relative susceptibility of hill slopes to the initiation sites of rainfall-triggered soil slip-debris flows in southwestern California. As such, the maps offer a partial answer to one part of the three parts necessary to predict the soil-slip/debris-flow process. A complete prediction of the process would include assessments of “where”, “when”, and “how big”. These maps empirically show part of the “where” of prediction (i.e., relative susceptibility to sites of initiation of the soil slips) but do not attempt to show the extent of run out of the resultant debris flows. Some information pertinent to “when” the process might begin is developed. “When” is determined mostly by dynamic factors such as rainfall rate and duration, for which local variations are not amenable to long-term prediction. “When” information is not provided on the maps but is described later in this narrative. The prediction of “how big” is addressed indirectly by restricting the maps to a single type of landslide process—soil slip-debris flows.
\nThe susceptibility maps were created through an iterative process from two kinds of information. First, locations of sites of past soil slips were obtained from inventory maps of past events. Aerial photographs, taken during six rainy seasons that produced abundant soil slips, were used as the basis for soil slip-debris flow inventory. Second, digital elevation models (DEM) of the areas that were inventoried were used to analyze the spatial characteristics of soil slip locations. These data were supplemented by observations made on the ground. Certain physical attributes of the locations of the soil-slip debris flows were found to be important and others were not. The most important attribute was the mapped bedrock formation at the site of initiation of the soil slip. However, because the soil slips occur in surficial materials overlying the bedrocks units, the bedrock formation can only serve as a surrogate for the susceptibility of the overlying surficial materials.
\nThe maps of susceptibility were created from those physical attributes learned to be important from the inventories. The multiple inventories allow a model to be created from one set of inventory data and evaluated with others. The resultant maps of relative susceptibility represent the best estimate generated from available inventory and DEM data.
\nSlope and aspect values used in the susceptibility analysis were 10-meter DEM cells at a scale of 1:24,000. For most of the area 10-meter DEMs were available; for those quadrangles that have only 30-meter DEMs, the 30-meter DEMS were resampled to 10-meters to maintain resolution of 10-meter cells. Geologic unit values used in the susceptibility analysis were five-meter cells. For convenience, the soil slip susceptibility values are assembled on 1:100,000-scale bases. Any area of the 1:100,000-scale maps can be transferred to 1:24,000-scale base without any loss of accuracy. Figure 32 is an example of part of a 1:100,000-scale susceptibility map transferred back to a 1:24,000-scale quadrangle.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Menlo Park, CA","doi":"10.3133/ofr0317","collaboration":"Prepared in cooperation with the California Geological Survey","usgsCitation":"Morton, D.M., Alvarez, R.M., Campbell, R., Bovard, K.R., Brown, D.T., Corriea, K.M., and Lesser, J.N., 2003, Preliminary soil-slip susceptibility maps, southwestern California: U.S. Geological Survey Open-File Report 2003-17, Report: 14 p.; 7 Plates: 41.0 x 36.0 inches or smaller; Readme; Metadata, https://doi.org/10.3133/ofr0317.","productDescription":"Report: 14 p.; 7 Plates: 41.0 x 36.0 inches or smaller; Readme; Metadata","numberOfPages":"46","additionalOnlineFiles":"Y","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":178312,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr0317.jpg"},{"id":4636,"rank":12,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2003/0017/","linkFileType":{"id":5,"text":"html"}},{"id":110376,"rank":13,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54144.htm","linkFileType":{"id":5,"text":"html"},"description":"54144"},{"id":285239,"rank":11,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/of/2003/0017/README.doc"},{"id":285250,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate7.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"}},{"id":285249,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate6.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"}},{"id":285248,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate5.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"}},{"id":285247,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate4.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"}},{"id":285246,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"}},{"id":285245,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"}},{"id":285244,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/plate1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"}},{"id":285240,"rank":3,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/of/2003/0017/sus_met.txt"},{"id":285238,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2003/0017/pdf/of03-17.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}}],"scale":"100000","projection":"Universal Transverse Mercator projection","country":"United States","state":"California","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -121.0,32.5 ], [ -121.0,35.5 ], [ -115.0,35.5 ], [ -115.0,32.5 ], [ -121.0,32.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c0ae","contributors":{"authors":[{"text":"Morton, Douglas M. scamp@usgs.gov","contributorId":4102,"corporation":false,"usgs":true,"family":"Morton","given":"Douglas","email":"scamp@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":242500,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Alvarez, Rachel M.","contributorId":74451,"corporation":false,"usgs":true,"family":"Alvarez","given":"Rachel","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":242503,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Campbell, Russell H.","contributorId":91074,"corporation":false,"usgs":true,"family":"Campbell","given":"Russell H.","affiliations":[],"preferred":false,"id":242505,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bovard, Kelly R.","contributorId":49009,"corporation":false,"usgs":true,"family":"Bovard","given":"Kelly","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":242502,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Brown, D. T.","contributorId":34196,"corporation":false,"usgs":true,"family":"Brown","given":"D.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":242501,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Corriea, K. M.","contributorId":81981,"corporation":false,"usgs":true,"family":"Corriea","given":"K.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":242504,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Lesser, J. N.","contributorId":102563,"corporation":false,"usgs":true,"family":"Lesser","given":"J.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":242506,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":47394,"text":"b2197 - 2003 - Velocity ratio and its application to predicting velocities","interactions":[],"lastModifiedDate":"2012-02-02T00:10:40","indexId":"b2197","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2197","title":"Velocity ratio and its application to predicting velocities","docAbstract":"The velocity ratio of water-saturated sediment derived from the Biot-Gassmann theory depends mainly on the Biot coefficient?a property of dry rock?for consolidated sediments\r\nwith porosity less than the critical porosity. With this theory, the shear moduli of dry sediments are the same as the shear moduli of water-saturated sediments. Because the velocity ratio depends on the Biot coefficient explicitly, Biot-Gassmann theory accurately predicts velocity ratios with respect to differential pressure for a given porosity. However, because the velocity ratio is weakly related to porosity, it is not appropriate to investigate the velocity ratio with respect to porosity (f).\r\nA new formulation based on the assumption that the velocity ratio is a function of (1?f)n yields a velocity ratio that depends on porosity, but not on the Biot coefficient explicitly. Unlike the Biot-Gassmann theory, the shear moduli of water-saturated sediments depend not only on the Biot coefficient but also on the pore fluid. This nonclassical behavior of the shear modulus of water-saturated sediment is speculated to be an effect of interaction between fluid and the solid matrix, resulting in softening or hardening of the rock frame and an effect of velocity dispersion owing to local fluid flow. The exponent n controls the degree of softening/hardening of the formation. Based on laboratory data measured near 1 MHz, this theory is extended to include the effect of differential pressure\r\non the velocity ratio by making n a function of differential pressure and consolidation. However, the velocity dispersion and anisotropy are not included in the formulation.","language":"ENGLISH","doi":"10.3133/b2197","usgsCitation":"Lee, M.W., 2003, Velocity ratio and its application to predicting velocities (Version 1.0): U.S. Geological Survey Bulletin 2197, 15 p., https://doi.org/10.3133/b2197.","productDescription":"15 p.","costCenters":[],"links":[{"id":170924,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":3974,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/bul/b2197/","linkFileType":{"id":5,"text":"html"}}],"edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a13e4b07f02db6022dd","contributors":{"authors":[{"text":"Lee, Myung W. mlee@usgs.gov","contributorId":779,"corporation":false,"usgs":true,"family":"Lee","given":"Myung","email":"mlee@usgs.gov","middleInitial":"W.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":235211,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":44635,"text":"wri024136 - 2003 - Simulation of ground-water/surface-water flow in the Santa Clara-Calleguas ground-water basin, Ventura County, California","interactions":[],"lastModifiedDate":"2026-03-11T20:26:01.827464","indexId":"wri024136","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4136","title":"Simulation of ground-water/surface-water flow in the Santa Clara-Calleguas ground-water basin, Ventura County, California","docAbstract":"Ground water is the main source of water in the Santa Clara-Calleguas ground-water basin that covers about 310 square miles in Ventura County, California. A steady increase in the demand for surface- and ground-water resources since the late 1800s has resulted in streamflow depletion and ground-water overdraft. This steady increase in water use has resulted in seawater intrusion, inter-aquifer flow, land subsidence, and ground-water contamination. The Santa Clara-Calleguas Basin consists of multiple aquifers that are grouped into upper- and lower-aquifer systems. The upper-aquifer system includes the Shallow, Oxnard, and Mugu aquifers. The lower-aquifer system includes the upper and lower Hueneme, Fox Canyon, and Grimes Canyon aquifers. The layered aquifer systems are each bounded below by regional unconformities that are overlain by extensive basal coarse-grained layers that are the major pathways for ground-water production from wells and related seawater intrusion. The aquifer systems are bounded below and along mountain fronts by consolidated bedrock that forms a relatively impermeable boundary to ground-water flow. Numerous faults act as additional exterior and interior boundaries to ground-water flow. The aquifer systems extend offshore where they crop out along the edge of the submarine shelf and within the coastal submarine canyons. Submarine canyons have dissected these regional aquifers, providing a hydraulic connection to the ocean through the submarine outcrops of the aquifer systems. Coastal landward flow (seawater intrusion) occurs within both the upper- and lower-aquifer systems. A numerical ground-water flow model of the Santa Clara-Calleguas Basin was developed by the U.S. Geological Survey to better define the geohydrologic framework of the regional ground-water flow system and to help analyze the major problems affecting water-resources management of a typical coastal aquifer system. Construction of the Santa Clara-Calleguas Basin model required the compilation of geographic, geologic, and hydrologic data and estimation of hydraulic properties and flows. The model was calibrated to historical surface-water and ground-water flow for the period 1891-1993. Sources of water to the regional ground-water flow system are natural and artificial recharge, coastal landward flow from the ocean (seawater intrusion), storage in the coarse-grained beds, and water from compaction of fine-grained beds (aquitards). Inflows used in the regional flow model simulation include streamflows routed through the major rivers and tributaries; infiltration of mountain-front runoff and infiltration of precipitation on bedrock outcrops and on valley floors; and artificial ground-water recharge of diverted streamflow, irrigation return flow, and treated sewage effluent. Most natural recharge occurs through infiltration (losses) of streamflow within the major rivers and tributaries and the numerous arroyos that drain the mountain fronts of the basin. Total simulated natural recharge was about 114,100 acre-feet per year (acre-ft/yr) for 1984-93: 27,800 acre-ft/yr of mountain-front and bedrock recharge, 24,100 acre-ft/yr of valley-floor recharge, and 62,200 acre-ft/yr of net streamflow recharge. Artificial recharge (spreading of diverted streamflow, irrigation return, and sewage effluent) is a major source of ground-water replenishment. During the 1984-93 simulation period, the average rate of artificial recharge at the spreading grounds was about 54,400 acre-ft/yr, 13 percent less than the simulated natural recharge rate for streamflow infiltration within the major rivers and tributaries. Estimated recharge from infiltration of irrigation return flow on the valley floors averaged about 51,000 acre-ft/yr, and treated sewage effluent averaged about 9,000 acre-ft/yr. Artificial recharge as streamflow diversion to the spreading grounds has occurred since 1929, and treated-sewage effluent has been discharged to stream channels since 1930. Under","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri024136","usgsCitation":"Hanson, R.T., Martin, P., and Koczot, K.M., 2003, Simulation of ground-water/surface-water flow in the Santa Clara-Calleguas ground-water basin, Ventura County, California: U.S. Geological Survey Water-Resources Investigations Report 2002-4136, 214 p., https://doi.org/10.3133/wri024136.","productDescription":"214 p.","costCenters":[],"links":[{"id":3726,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri024136/text.html","linkFileType":{"id":5,"text":"html"}},{"id":169012,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f7e4b07f02db5f231f","contributors":{"authors":[{"text":"Hanson, Randall T. 0000-0002-9819-7141 rthanson@usgs.gov","orcid":"https://orcid.org/0000-0002-9819-7141","contributorId":801,"corporation":false,"usgs":true,"family":"Hanson","given":"Randall","email":"rthanson@usgs.gov","middleInitial":"T.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":230154,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Martin, Peter pmmartin@usgs.gov","contributorId":799,"corporation":false,"usgs":true,"family":"Martin","given":"Peter","email":"pmmartin@usgs.gov","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":230153,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Koczot, Kathryn M. 0000-0001-5728-9798 kmkoczot@usgs.gov","orcid":"https://orcid.org/0000-0001-5728-9798","contributorId":2039,"corporation":false,"usgs":true,"family":"Koczot","given":"Kathryn","email":"kmkoczot@usgs.gov","middleInitial":"M.","affiliations":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"preferred":true,"id":230155,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":53727,"text":"ofr2003476 - 2003 - Effects of channel modification on fish habitat in the upper Yellowstone River: Final report to the USACE, Omaha","interactions":[],"lastModifiedDate":"2016-05-23T11:31:18","indexId":"ofr2003476","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2003-476","title":"Effects of channel modification on fish habitat in the upper Yellowstone River: Final report to the USACE, Omaha","docAbstract":"A two-dimensional hydrodynamic simulation model was coupled with a geographic information system (GIS) to produce a variety of habitat classification maps for three study reaches in the upper Yellowstone River basin in Montana. Data from these maps were used to examine potential effects of channel modification on shallow, slow current velocity (SSCV) habitats that are important refugia and nursery areas for young salmonids. At low flows, channel modifications were found to contribute additional SSCV habitat, but this contribution was negligible at higher discharges. During runoff, when young salmonids are most vulnerable to downstream displacement, the largest areas of SSCV habitat occurred in side channels, point bars, and overbank areas. Because of the diversity of elevations in the existing Yellowstone River, SSCV habitat tends to be available over a wide range of discharges. Based on simulations in modified and unmodified sub-reaches, channel simplification results in decreased availability of SSCV habitat, particularly during runoff. The combined results of the fish population and fish habitat studies present strong evidence that during runoff, SSCV habitat is most abundant in side channel and overbank areas and that juvenile salmonids use these habitats as refugia. Channel modifications that result in reduced availability of side channel and overbank habitats, particularly during runoff, will probably cause local reductions in juvenile abundances during the runoff period. Effects of reduced juvenile abundances during runoff on adult numbers later in the year will depend on (1) the extent of channel modification, (2) patterns of fish displacement and movement, (3) longitudinal connectivity between reaches that contain refugia and those that do not, and (4) the relative importance of other limiting factors.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr2003476","usgsCitation":"Bowen, Z.H., Bovee, K.D., and Waddle, T.J., 2003, Effects of channel modification on fish habitat in the upper Yellowstone River: Final report to the USACE, Omaha: U.S. Geological Survey Open-File Report 2003-476, 80 p., https://doi.org/10.3133/ofr2003476.","productDescription":"80 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"links":[{"id":179438,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr2003476.PNG"},{"id":320297,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2003/0476/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Montana","county":"Park County","otherGeospatial":"Yellowstone River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.74905395507812,\n 45.32704768567264\n ],\n [\n -110.61721801757812,\n 45.41966030640988\n ],\n [\n -110.54855346679686,\n 45.596743928454124\n ],\n [\n -110.49636840820312,\n 45.69850658738848\n ],\n [\n -110.52932739257812,\n 45.71097418682748\n ],\n [\n -110.59112548828125,\n 45.64092778836502\n ],\n [\n -110.60623168945312,\n 45.55444852652113\n ],\n [\n -110.64468383789062,\n 45.487094732298374\n ],\n [\n -110.65704345703124,\n 45.433153642271414\n ],\n [\n -110.69549560546874,\n 45.42737117898911\n ],\n [\n -110.77239990234375,\n 45.346354488594436\n ],\n [\n -110.74905395507812,\n 45.32704768567264\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2fe4b07f02db61629c","contributors":{"authors":[{"text":"Bowen, Zachary H. 0000-0002-8656-1831 bowenz@usgs.gov","orcid":"https://orcid.org/0000-0002-8656-1831","contributorId":821,"corporation":false,"usgs":true,"family":"Bowen","given":"Zachary","email":"bowenz@usgs.gov","middleInitial":"H.","affiliations":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"preferred":true,"id":248241,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bovee, Ken D.","contributorId":100447,"corporation":false,"usgs":true,"family":"Bovee","given":"Ken","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":248243,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waddle, Terry J.","contributorId":43430,"corporation":false,"usgs":true,"family":"Waddle","given":"Terry","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":248242,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1015288,"text":"1015288 - 2003 - Effects of river flow regime on cottonwood leaf litter dynamics in semi-arid northwestern Colorado","interactions":[],"lastModifiedDate":"2017-12-26T12:27:21","indexId":"1015288","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3451,"text":"Southwestern Naturalist","active":true,"publicationSubtype":{"id":10}},"title":"Effects of river flow regime on cottonwood leaf litter dynamics in semi-arid northwestern Colorado","docAbstract":"We compared production and breakdown of Fremont cottonwood (Populus deltoides wislizenii) leaf litter at matched floodplain sites on the regulated Green River and unregulated Yampa River in semi-arid northwestern Colorado. Litter production under trees was similar at sites in 1999 (250 g/m2, oven-dry) but lower in 2000 (215 and 130 g/m2), a drought year that also featured an outbreak of defoliating beetles at the Yampa River site. Our production values were similar to the few others reported for riparian forests within semi-arid or arid areas. Leaf litter in portions of the floodplain not inundated during the spring flood lost organic matter at the same rate as leaves placed in upland sites in 1998 and 2000: 35 to 50% of organic matter during an approximately 160-day spring and summer period. Inundated litter lost 55 to 90% of its organic matter during the same period. Organic matter loss from inundated leaves increased with duration of inundation and with deposition of fine sediment. Pooled across locations, leafpack data suggested that nitrogen concentration (mg N/kg organic matter) increased until about 65% of the initial organic matter was lost. This increase likely reflected the buildup of microbial decomposer populations. The role of insects and other macroinvertebrates in litter breakdown apparently was minor at both sites. Large spatial and temporal variation in litter dynamics in aridland floodplain settings is ensured by microtopographic variation in the alluvial surface coupled with year-to-year variation associated with most natural flood regimes. Factors reducing flood flow frequency or magnitude will reduce overall breakdown rates on the floodplain towards those found in drier upland environments.
","language":"English","publisher":"Southwestern Association of Naturalists","doi":"10.1894/0038-4909(2003)048<0188:EORFRO>2.0.CO;2","usgsCitation":"Andersen, D., and Nelson, S.M., 2003, Effects of river flow regime on cottonwood leaf litter dynamics in semi-arid northwestern Colorado: Southwestern Naturalist, v. 48, no. 2, p. 188-201, https://doi.org/10.1894/0038-4909(2003)048<0188:EORFRO>2.0.CO;2.","productDescription":"14 p.","startPage":"188","endPage":"201","costCenters":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"links":[{"id":132416,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"48","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a28e4b07f02db611609","contributors":{"authors":[{"text":"Andersen, D.C.","contributorId":19119,"corporation":false,"usgs":true,"family":"Andersen","given":"D.C.","email":"","affiliations":[],"preferred":false,"id":322769,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nelson, S. M.","contributorId":81853,"corporation":false,"usgs":false,"family":"Nelson","given":"S.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":322770,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":53273,"text":"ofr2003222 - 2003 - Reconnaissance-level application of physical habitat simulation in the evaluation of physical habitat limits in the Animas Basin, Colorado","interactions":[],"lastModifiedDate":"2016-05-23T11:17:50","indexId":"ofr2003222","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2003-222","title":"Reconnaissance-level application of physical habitat simulation in the evaluation of physical habitat limits in the Animas Basin, Colorado","docAbstract":"The Animas River is in southwestern Colorado and flows mostly to the south to join the San Juan River at Farmington, New Mexico (Figure 1). The Upper Animas River watershed is in San Juan County, Colorado and is located in the San Juan Mountains. The lower river is in the Colorado Plateau country. The winters are cold with considerable snowfall and little snowmelt in the mountains in the upper part of the basin. The lower basin has less snow but the winters are still cold. The streamflows during the winter are low and reasonably stable.
\nThe native trout in the Animas Basin is the cutthroat trout. Few native trout remain and the trout found in the upper watershed are brook trout with rainbow and brown trout in the lower river. There is considerable metal contamination in the upper basin near Silverton but a brook trout fishery does exist in the Animas River from just above Howardsville to where the Animas joins Cement Creek in Silverton.
\nThere are two principle objectives of the habitat studies in the Animas Basin: (1) to improve understanding of the fate of sediment from mining operations from the view point of physical habitat impacts, and (2) to determine if reconnaissance level physical habitat studies can be useful in understanding the impacts of mining on the aquatic ecosystem.
\nPart of the project was to apply the Physical Habitat Simulation System (PHABSIM) to selected locations in the Upper Animas River Basin, Colorado in order to demonstrate the importance of physical habitat in evaluating the efficacy of mined land remediation activities. Physical habitat analysis included the use of sedimentation variables in physical habitat simulations. A map of the Upper Animas Basin is presented in Figure 2.
\nThe project involves collecting data for the following locations: Animas River above Magee Creek; Animas River above Howardsville; Animas River below Howardsville; Animas River above Silverton at Hillsdale Cemetery; Animas River at Silverton; Cement Creek above Silverton; Cement Creek at Silverton; Mineral Creek at Powerline above Silverton; Mineral Creek at Campground; South Mineral Creek at Overflow Campground; Mineral Creek above Bear Creek; Mineral Creek at Silverton; Animas River below Silverton; and Animas River at Elk Park.
\nBed material samples were collected at each site. These included samples of the armour, the substrate, and sand and fines deposited on the surface. At selected sites the stream morphology was measured. These measurements included one to three cross sections, stream discharge, and water surface elevations. The data are located in the files of the Fort Collins Science Center.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr2003222","usgsCitation":"Milhous, R.T., 2003, Reconnaissance-level application of physical habitat simulation in the evaluation of physical habitat limits in the Animas Basin, Colorado: U.S. Geological Survey Open-File Report 2003-222, v, 16 p., https://doi.org/10.3133/ofr2003222.","productDescription":"v, 16 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"links":[{"id":177987,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr2003222.PNG"},{"id":320296,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2003/0222/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Colorado, New Mexico","otherGeospatial":"Animas River Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.21807861328125,\n 36.697053200100335\n ],\n [\n -107.940673828125,\n 36.82247761166621\n ],\n [\n -107.74566650390625,\n 37.2587521486561\n ],\n [\n -107.53692626953125,\n 37.861844098370945\n ],\n [\n -107.611083984375,\n 37.93553306183642\n ],\n [\n -107.82257080078125,\n 37.85750715625203\n ],\n [\n -107.99835205078124,\n 37.54022177661216\n ],\n [\n -108.03131103515625,\n 37.24782120155428\n ],\n [\n -108.0670166015625,\n 37.00035919622158\n ],\n [\n -108.21807861328125,\n 36.697053200100335\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a49e4b07f02db623b5f","contributors":{"authors":[{"text":"Milhous, Robert T.","contributorId":28646,"corporation":false,"usgs":true,"family":"Milhous","given":"Robert","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":247141,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":93828,"text":"93828 - 2003 - Sedimentation rates in the marshes of Sand Lake National Wildlife Refuge","interactions":[],"lastModifiedDate":"2017-10-26T10:55:23","indexId":"93828","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":9,"text":"Other Report"},"title":"Sedimentation rates in the marshes of Sand Lake National Wildlife Refuge","docAbstract":"Impoundments located within river systems in the Northern Great Plains are vulnerable to sediment inputs because intensive agriculture in watersheds has increased soil erosion and sediments in rivers. At the request of the U.S. Fish and Wildlife Service (FWS), we evaluated the vertical accretion of sediment in the Mud Lake impoundment of Sand Lake National Wildlife Refuge (NWR), Brown County, South Dakota. The Mud Lake impoundment was created in 1936 by constructing a low-head dam across the James River. We collected sediment cores from the Mud Lake impoundment during August 2000 for determination of vertical accretion rates. Accretion rates were estimated using cesium-13 7 and lead-210 isotopic dating techniques to estimate sediment accretion over the past 100 years. Accretion rates were greatest near the dam (1.3 cm yr-1) with less accretion (0.2 cm yr-1) occurring in the upper reaches of Mud Lake. As expected, accretion was highest near the dam where water velocities and greater water depth facilitates sediment deposition. Higher rates of sedimentation (accretion> 2.0 cm year-1) occurred during the 1990s when river flows were especially high. Since 1959, sediment accretion has reduced maximum pool depth of Mud Lake near the dam by 55 cm. Assuming that sediment accretion rates remain the same in the future, we project Mud Lake will have a maximum pool depth of 77 and 51 cm by 2020 and 2040, respectively. Over this same time frame, water depths in the upper reaches of Mud Lake would be reduced to< 2 cm. Projected future loss of water depth will severely limit the ability of managers to manipulate pool levels in Mud Lake to cycle vegetation and create interspersion of cover and water to meet current wildlife habitat management objectives. As predicted for major dams constructed on rivers throughout the world, Mud Lake will have a finite life span. Our data suggests that the functional life span of Mud Lake since construction will be < 100 years. We anticipate that over the next 20 years, sediments entering Mud Lake will reduce water depths to the point that current wildlife management objectives cannot be achieved through customary water-level manipulations. Sedimentation impacts are not unique to the Sand Lake NWR. It is widely accepted that impoundments trap sediments and shallow impoundments, such as those managed by the FWS, are especially vulnerable. Given the ecological impacts associated with loss of water depths, we recommend that managers begin evaluating the long-term wildlife management goals for the refuge relative to associated costs and feasibility of options available to enhance and maximize the life span of existing impoundments, including upper watershed management.
","language":"English","publisher":"U.S. Geological Survey, Northern Prairie Wildlife Research Center","publisherLocation":"Jamestown, ND","usgsCitation":"Gleason, R., Euliss, N., and Holmes, C.W., 2003, Sedimentation rates in the marshes of Sand Lake National Wildlife Refuge, 27 p.","productDescription":"27 p.","costCenters":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":128384,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -98.31939697265625,\n 45.71672752568247\n ],\n [\n -98.1793212890625,\n 45.71672752568247\n ],\n [\n -98.1793212890625,\n 45.84219445795288\n ],\n [\n -98.31939697265625,\n 45.84219445795288\n ],\n [\n -98.31939697265625,\n 45.71672752568247\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ae4b07f02db5fbc54","contributors":{"authors":[{"text":"Gleason, R.A.","contributorId":46035,"corporation":false,"usgs":true,"family":"Gleason","given":"R.A.","email":"","affiliations":[],"preferred":false,"id":298001,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Euliss, N.H. Jr.","contributorId":54917,"corporation":false,"usgs":true,"family":"Euliss","given":"N.H.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":298002,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Holmes, C. W.","contributorId":36076,"corporation":false,"usgs":true,"family":"Holmes","given":"C.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":298000,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70024968,"text":"70024968 - 2003 - Percolation induced heat transfer in deep unsaturated zones","interactions":[],"lastModifiedDate":"2012-03-12T17:20:05","indexId":"70024968","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2327,"text":"Journal of Geotechnical and Geoenvironmental Engineering","active":true,"publicationSubtype":{"id":10}},"title":"Percolation induced heat transfer in deep unsaturated zones","docAbstract":"Subsurface temperature data from a borehole located in a desert wash were measured and used to delineate the conductive and advective heat transfer regimes, and to estimate the percolation quantity associated with the 1997-1998 El Ni??no precipitation. In an arid environment, conductive heat transfer dominates the variation of shallow subsurface temperature most of the time, except during sporadic precipitation periods. The subsurface time-varying temperature due to conductive heat transfer is highly correlated with the surface atmospheric temperature variation, whereas temperature variation due to advective heat transfer is strongly correlated with precipitation events. The advective heat transfer associated with precipitation and infiltration is the focus of this paper. Disruptions of the subsurface conductive temperature regime, associated with the 1997-1998 El Ni??no precipitation, were detected and used to quantify the percolation quantity. Modeling synthesis using a one-dimensional coupled heat and unsaturated flow model indicated that a percolation per unit area of 0.7 to 1.3 m height of water in two weeks during February 1998 was responsible for the observed temperature deviations down to a depth of 35.2 m. The reported study demonstrated quantitatively, for the first time, that the near surface temperature variation due to advective heat transfer can be significant at a depth greater than 10 m in unsaturated soils and can be used to infer the percolation amount in thick unsaturated soils.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Geotechnical and Geoenvironmental Engineering","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1061/(ASCE)1090-0241(2003)129:11(1040)","issn":"10900241","usgsCitation":"Lu, N., and LeCain, G., 2003, Percolation induced heat transfer in deep unsaturated zones: Journal of Geotechnical and Geoenvironmental Engineering, v. 129, no. 11, p. 1040-1053, https://doi.org/10.1061/(ASCE)1090-0241(2003)129:11(1040).","startPage":"1040","endPage":"1053","numberOfPages":"14","costCenters":[],"links":[{"id":207840,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1061/(ASCE)1090-0241(2003)129:11(1040)"},{"id":233079,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"129","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a7676e4b0c8380cd7811b","contributors":{"authors":[{"text":"Lu, N.","contributorId":96025,"corporation":false,"usgs":true,"family":"Lu","given":"N.","email":"","affiliations":[],"preferred":false,"id":403288,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"LeCain, G.D.","contributorId":22810,"corporation":false,"usgs":true,"family":"LeCain","given":"G.D.","affiliations":[],"preferred":false,"id":403287,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70025705,"text":"70025705 - 2003 - Modeling flow and transport in unsaturated fractured rock: An evaluation of the continuum approach","interactions":[],"lastModifiedDate":"2018-09-25T08:43:53","indexId":"70025705","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2003","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2233,"text":"Journal of Contaminant Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"Modeling flow and transport in unsaturated fractured rock: An evaluation of the continuum approach","docAbstract":"Because the continuum approach is relatively simple and straightforward to implement, it has been commonly used in modeling flow and transport in unsaturated fractured rock. However, the usefulness of this approach can be questioned in terms of its adequacy for representing fingering flow and transport in unsaturated fractured rock. The continuum approach thus needs to be evaluated carefully by comparing simulation results with field observations directly related to unsaturated flow and transport processes. This paper reports on such an evaluation, based on a combination of model calibration and prediction, using data from an infiltration test carried out in a densely fractured rock within the unsaturated zone of Yucca Mountain, Nevada. Comparisons between experimental and modeling results show that the continuum approach may be able to capture important features of flow and transport processes observed from the test. The modeling results also show that matrix diffusion may have a significant effect on the overall transport behavior in unsaturated fractured rocks, which can be used to estimate effective fracture-matrix interface areas based on tracer transport data. While more theoretical, numerical, and experimental studies are needed to provide a conclusive evaluation, this study suggests that the continuum approach is useful for modeling flow and transport in unsaturated, densely fractured rock. ?? 2002 Elsevier Science B.V. All rights reserved.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Contaminant Hydrology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1016/S0169-7722(02)00170-5","issn":"01697722","usgsCitation":"Liu, H., Haukwa, C., Ahlers, C., Bodvarsson, G., Flint, A.L., and Guertal, W., 2003, Modeling flow and transport in unsaturated fractured rock: An evaluation of the continuum approach: Journal of Contaminant Hydrology, v. 62-63, p. 173-188, https://doi.org/10.1016/S0169-7722(02)00170-5.","startPage":"173","endPage":"188","numberOfPages":"16","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":478404,"rank":10000,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://digital.library.unt.edu/ark:/67531/metadc776968/","text":"External Repository"},{"id":234564,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":208666,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/S0169-7722(02)00170-5"}],"volume":"62-63","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5bf9e4b0c8380cd6f941","contributors":{"authors":[{"text":"Liu, H.-H.","contributorId":14618,"corporation":false,"usgs":true,"family":"Liu","given":"H.-H.","email":"","affiliations":[],"preferred":false,"id":406242,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Haukwa, C.B.","contributorId":28415,"corporation":false,"usgs":true,"family":"Haukwa","given":"C.B.","email":"","affiliations":[],"preferred":false,"id":406243,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ahlers, C.F.","contributorId":77336,"corporation":false,"usgs":true,"family":"Ahlers","given":"C.F.","email":"","affiliations":[],"preferred":false,"id":406245,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bodvarsson, G.S.","contributorId":98045,"corporation":false,"usgs":true,"family":"Bodvarsson","given":"G.S.","email":"","affiliations":[],"preferred":false,"id":406246,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Flint, A. L.","contributorId":102453,"corporation":false,"usgs":true,"family":"Flint","given":"A.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":406247,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Guertal, W.B.","contributorId":74553,"corporation":false,"usgs":true,"family":"Guertal","given":"W.B.","email":"","affiliations":[],"preferred":false,"id":406244,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ]}