This report presents selected low-flow and flow-duration characteristics for 386 sites throughout Ohio. These sites include 195 long-term continuous- record stations with streamflow data through water year 1997 (October 1 to September 30) and for 191 low-flow partial-record stations with measurements into water year 1999. The characteristics presented for the long-term continuous-record stations are minimum daily streamflow; average daily streamflow; harmonic mean flow; 1-, 7-, 30-, and 90-day minimum average low flow with 2-, 5-, 10-, 20-, and 50-year recurrence intervals; and 98-, 95-, 90-, 85-, 80-, 75-, 70-, 60-, 50-, 40-, 30-, 20-, and 10-percent daily duration flows. The characteristics presented for the low-flow partial-record stations are minimum observed streamflow; estimated 1-, 7-, 30-, and 90-day minimum average low flow with 2-, 10-, and 20-year recurrence intervals; and estimated 98-, 95-, 90-, 85- and 80-percent daily duration flows. The low-flow frequency and duration analyses were done for three seasonal periods (warm weather, May 1 to November 30; winter, December 1 to February 28/29; and autumn, September 1 to November 30), plus the annual period based on the climatic year (April 1 to March 31).
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri014140","collaboration":"Prepared in cooperation with the Ohio Department of Natural Resources, Division of Water","usgsCitation":"Straub, D.E., 2001, Low-flow characteristics of streams in Ohio through water year 1997: U.S. Geological Survey Water-Resources Investigations Report 2001–4140, iv, 415 p., https://doi.org/10.3133/wri014140.","productDescription":"iv, 415 p.","numberOfPages":"423","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":513,"text":"Ohio Water Science Center","active":true,"usgs":true}],"links":[{"id":161258,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2001/4140/coverthb.jpg"},{"id":362961,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4140/wri20014140.pdf","text":"Report","size":"20.9 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 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\"}}]}","contact":"Director, Ohio Water Science Center
U.S. Geological Survey
6460 Busch Blvd.
Columbus, OH 43229-1737
The Kiowa core was obtained as a component of the Denver Basin Project, a cooperative research effort to study the evolution of the Denver Basin, Colorado. The Kiowa core provides a virtually continuous stratigraphic record of the Upper Cretaceous and lower Tertiary strata of the Denver Basin. The upper portion of the core recovered strata conventionally referred to as the Arapahoe and Denver Formations and the Dawson Arkose. A prominent unconformity marked by a mature paleosol breaks these strata into two unconformity-bounded sequences; the lower sequence is termed Dl and the upper sequence, D2. Beneath these units and also penetrated by the core occur the Laramie Formation, Fox Hills Sandstone, and Pierre Shale.
The site for coring was selected in order to obtain fine-grained strata suitable for both palynological and paleomagnetic analyses. The coring effort recovered 93 percent of the 2,256 ft of rock penetrated, resulting in a nearly continuous record of the sedimentary rocks recording the retreat of the Cretaceous Interior Seaway and the subsequent uplift of the Front Range portion of the Rocky Mountains.
Palynological data constrain the Cretaceous-Tertiary boundary to a depth between 878 and 880 ft in the core. The palynological data also serve to bracket the age of the paleosol marking the unconformity between the Dl and D2 sequences to between middle Paleocene and earliest Eocene. The paleomagnetic data are interpreted to represent polarity intervals ranging from polarity subchrons 31r to 28n and polarity subchron 24r.
Hydrologic analyses indicate variable aquifer characteristics across the State-defined bedrock aquifers. Individual aquifer units exhibit generally lower water-yield potential than was identified to the west in a core drilled by the U.S. Geological Survey (USGS) in 1987 at Castle Pines, Colorado. Downhole temperature measurements indicate a normal geothermal gradient of 30°C/ km. Perturbations of the gradient may represent active fluid flow through the aquifers penetrated by the core.
Petrographic examination of the cored sandstone and mudstone units document both the clay-rich character of the paleosol series marking the boundary between the Dl and D2 sequences, and variation in sandstone composition with depth. The lower sequence (Dl) is characterized by litharenites with a significant volcaniclastic component, while the upper sequence (D2) is more arkosic. Extensive lignite beds occur in Dl in the cored interval and these appear as strong reflectors on the seismic line that passes near the core hole. A set of electric logs, core descriptions, and derived data sets accompany this report.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr01185","collaboration":"Prepared in cooperation with National Science Foundation, U.S. Geological Survey, Colorado Department of Natural Resources, Division of Water Resources, Office of the State Engineer, Colorado Geological Survey, Elbert County, Colorado, Colorado State University, University of Colorado, New Mexico Institute of Mining and Technology, University of Alaska, Scripps Institution of Oceanography","usgsCitation":"Raynolds, R.G., Johnson, K.R., Arnold, L., Farnham, T.M., Fleming, R., Hicks, J.F., Kelley, S.A., Lapey, L.A., Nichols, D.J., Obradovich, J.D., and Wilson, M., 2001, The Kiowa core, a continuous drill core through the Denver Basin bedrock aquifers at Kiowa, Elbert County, Colorado (Version 1.0): U.S. Geological Survey Open-File Report 2001-185, 127 p., https://doi.org/10.3133/ofr01185.","productDescription":"127 p.","costCenters":[],"links":[{"id":2932,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2001/ofr-01-0185/","linkFileType":{"id":5,"text":"html"}},{"id":161292,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2001/0185/report-thumb.jpg"},{"id":59728,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2001/0185/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Colorado","county":"Elbert County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -104.51053619384766,\n 39.319159627523035\n ],\n [\n -104.42161560058594,\n 39.319159627523035\n ],\n [\n -104.42161560058594,\n 39.37756814810105\n ],\n [\n -104.51053619384766,\n 39.37756814810105\n ],\n [\n -104.51053619384766,\n 39.319159627523035\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c03e","contributors":{"authors":[{"text":"Raynolds, Robert G.H.","contributorId":70814,"corporation":false,"usgs":true,"family":"Raynolds","given":"Robert","email":"","middleInitial":"G.H.","affiliations":[],"preferred":false,"id":205607,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, Kirk R.","contributorId":16877,"corporation":false,"usgs":true,"family":"Johnson","given":"Kirk","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":205602,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Arnold, L. Rick","contributorId":101613,"corporation":false,"usgs":true,"family":"Arnold","given":"L. Rick","affiliations":[],"preferred":false,"id":205611,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Farnham, Timothy M.","contributorId":44202,"corporation":false,"usgs":true,"family":"Farnham","given":"Timothy","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":205605,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Fleming, R. Farley","contributorId":83950,"corporation":false,"usgs":true,"family":"Fleming","given":"R. Farley","affiliations":[],"preferred":false,"id":205608,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Hicks, Jason F.","contributorId":52235,"corporation":false,"usgs":true,"family":"Hicks","given":"Jason","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":205606,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Kelley, Shari A.","contributorId":25606,"corporation":false,"usgs":true,"family":"Kelley","given":"Shari","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":205604,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Lapey, Laura A.","contributorId":103332,"corporation":false,"usgs":true,"family":"Lapey","given":"Laura","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":205612,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Nichols, Douglas J.","contributorId":87184,"corporation":false,"usgs":true,"family":"Nichols","given":"Douglas","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":205610,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Obradovich, John D.","contributorId":84361,"corporation":false,"usgs":true,"family":"Obradovich","given":"John","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":205609,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Wilson, Michael D.","contributorId":23188,"corporation":false,"usgs":true,"family":"Wilson","given":"Michael D.","affiliations":[],"preferred":false,"id":205603,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":30941,"text":"wri014155 - 2001 - Evaluation of the streamflow-gaging network of Texas and a proposed core network","interactions":[],"lastModifiedDate":"2017-01-12T12:42:39","indexId":"wri014155","displayToPublicDate":"2001-10-01T00:00:00","publicationYear":"2001","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":"2001-4155","title":"Evaluation of the streamflow-gaging network of Texas and a proposed core network","docAbstract":"The U.S. Geological Survey streamflowgaging\r\nnetwork in Texas is operated as part of the\r\nNational Streamgaging Program and is jointly\r\nfunded by the Geological Survey and Federal,\r\nState, and local agencies. This report documents an\r\nevaluation of the existing (as of October 1, 1999)\r\nnetwork with regard to four major objectives of\r\nstreamflow data; and on the basis of that evaluation,\r\nproposes a core network of streamflowgaging\r\nstations that best meets those objectives.\r\nThe objectives are (1) regionalization (estimate\r\nflows or flow characteristics at ungaged sites in\r\n11 hydrologically similar regions), (2) major flow\r\n(obtain flow rates and volumes in large streams),\r\n(3) outflow from the State (account for streamflow\r\nleaving the State), and (4) streamflow conditions\r\nassessment (assess current conditions with regard\r\nto long-term data, and define temporal trends in\r\nflow). The network analysis resulted in a proposed\r\ncore network of 263 stations. Of those 263 stations,\r\n43 were discontinued as of October 1, 1999, and\r\n15 were partial-record stations. Fifty-five of the\r\nproposed core-network stations meet two of the\r\nfour major objectives, 16 stations meet three objectives,\r\nand 1 station meets all four. One-hundred\r\neighty-five stations with a median record length of\r\n33 years were selected to meet the regionalization\r\nobjective. Ninety-two stations with a median\r\nrecord length of about 62 years were selected to\r\nmeet the major-flow objective. Twenty-six stations\r\nwith a median record length of 59 years were\r\nselected to meet the outflow from the State objective.\r\nFifty stations with a median record length of\r\n53 years were selected to meet the streamflow conditions\r\nassessment objective.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri014155","collaboration":"In cooperation with the Texas Water Development Board","usgsCitation":"Slade, R.M., Howard, T., and Anaya, R., 2001, Evaluation of the streamflow-gaging network of Texas and a proposed core network: U.S. Geological Survey Water-Resources Investigations Report 2001-4155, HTML Document; Report: iv, 40 p.; Plate: 26 x 26 inches, https://doi.org/10.3133/wri014155.","productDescription":"HTML Document; Report: iv, 40 p.; Plate: 26 x 26 inches","costCenters":[{"id":583,"text":"Texas Water Science 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5f9fe9","contributors":{"authors":[{"text":"Slade, Raymond M. Jr.","contributorId":46487,"corporation":false,"usgs":true,"family":"Slade","given":"Raymond","suffix":"Jr.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":204405,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Howard, Teresa","contributorId":65516,"corporation":false,"usgs":true,"family":"Howard","given":"Teresa","email":"","affiliations":[],"preferred":false,"id":204406,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Anaya, Roberto","contributorId":10827,"corporation":false,"usgs":true,"family":"Anaya","given":"Roberto","email":"","affiliations":[],"preferred":false,"id":204404,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30937,"text":"wri014142 - 2001 - Estimated flow-duration curves for selected ungaged sites in Kansas","interactions":[],"lastModifiedDate":"2012-02-02T00:09:12","indexId":"wri014142","displayToPublicDate":"2001-10-01T00:00:00","publicationYear":"2001","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":"2001-4142","title":"Estimated flow-duration curves for selected ungaged sites in Kansas","docAbstract":"Flow-duration curves for 1968-98 were estimated for 32 ungaged sites in the Missouri, Smoky Hill-Saline, Solomon, Marais des Cygnes, Walnut, Verdigris, and Neosho River Basins in Kansas. Also included from a previous report are estimated flow-duration curves for 16 ungaged sites in the Cimarron and lower Arkansas River Basins in Kansas. The method of estimation used six unique factors of flow duration: (1) mean streamflow and percentage duration of mean streamflow, (2) ratio of 1-percent-duration streamflow to mean streamflow, (3) ratio of 0.1-percent-duration streamflow to 1-percent-duration streamflow, (4) ratio of 50-percent-duration streamflow to mean streamflow, (5) percentage duration of appreciable streamflow (0.10 cubic foot per second), and (6) average slope of the flow-duration curve. These factors were previously developed from a regionalized study of flow-duration curves using streamflow data for 1921-76 from streamflow-gaging stations with drainage areas of 100 to 3,000 square miles. The method was tested on a currently (2001) measured, continuous-record streamflow-gaging station on Salt Creek near Lyndon, Kansas, with a drainage area of 111 square miles and was found to adequately estimate the computed flow-duration curve for the station. The method also was tested on a currently (2001) measured, continuous-record, streamflow-gaging station on Soldier Creek near Circleville, Kansas, with a drainage area of 49.3 square miles. The results of the test on Soldier Creek near Circleville indicated that the method could adequately estimate flow-duration curves for sites with drainage areas of less than 100 square miles. The low-flow parts of the estimated flow-duration curves were verified or revised using 137 base-flow discharge measurements made during 1999-2000 at the 32 ungaged sites that were correlated with base-flow measurements and flow-duration analyses performed at nearby, long-term, continuous-record, streamflow-gaging stations (index stations). The method did not adequately estimate the flow-duration curves for two sites in the western one-third of the State because of substantial changes in farming practices (terracing and intensive ground-water withdrawal) that were not accounted for in the two previous studies (Furness, 1959; Jordan, 1983). For these two sites, there was enough historic, continuous-streamflow record available to perform record-extension techniques correlated to their respective index stations for the development of the estimated flow-duration curves. The estimated flow-duration curves at the ungaged sites can be used for projecting future flow frequencies for assessment of total maximum daily loads (TMDLs) or other water-quality constituents, water-availability studies, and for basin-characteristic studies. ","language":"ENGLISH","doi":"10.3133/wri014142","usgsCitation":"Studley, S., 2001, Estimated flow-duration curves for selected ungaged sites in Kansas: U.S. Geological Survey Water-Resources Investigations Report 2001-4142, 90 p. , https://doi.org/10.3133/wri014142.","productDescription":"90 p. ","costCenters":[],"links":[{"id":2909,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wrir014142","linkFileType":{"id":5,"text":"html"}},{"id":95885,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4142/report.pdf","size":"20444","linkFileType":{"id":1,"text":"pdf"}},{"id":161259,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2001/4142/report-thumb.jpg"},{"id":13766,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://ks.water.usgs.gov/pubs/reports/wrir.01-4142.html","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e478fe4b07f02db48a3cf","contributors":{"authors":[{"text":"Studley, S.E.","contributorId":13662,"corporation":false,"usgs":true,"family":"Studley","given":"S.E.","affiliations":[],"preferred":false,"id":204398,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30916,"text":"wri014074 - 2001 - Methods to quantify seepage beneath Levee 30, Miami-Dade County, Florida","interactions":[],"lastModifiedDate":"2023-03-15T18:51:36.439002","indexId":"wri014074","displayToPublicDate":"2001-10-01T00:00:00","publicationYear":"2001","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":"2001-4074","title":"Methods to quantify seepage beneath Levee 30, Miami-Dade County, Florida","docAbstract":"A two-dimensional, cross-sectional, finite-difference, ground-water flow model and a simple application of Darcy?s law were used to quantify ground-water flow (from a wetlands) beneath Levee 30 in Miami-Dade County, Florida. Geologic and geophysical data, vertical seepage data from the wetlands, canal discharge data, ground-water-level data, and surface-water-stage data collected during 1995 and 1996 were used as boundary conditions and calibration data for the ground-water flow model and as input for the analytical model. Vertical seepage data indicated that water from the wetlands infiltrated the subsurface, near Levee 30, at rates ranging from 0.033 to 0.266 foot per day when the gates at the control structures along Levee 30 canal were closed. During the same period, stage differences between the wetlands (Water Conservation Area 3B) and Levee 30 canal ranged from 0.11 to 1.27 feet. A layer of low-permeability limestone, located 7 to 10 feet below land surface, restricts vertical flow between the surface water in the wetlands and the ground water. Based on measured water-level data, ground-water flow appears to be generally horizontal, except in the direct vicinity of the canal. The increase in discharge rate along a 2-mile reach of the Levee 30 canal ranged from 9 to 30 cubic feet per second per mile and can be attributed primarily to ground-water inflow. Flow rates in Levee 30 canal were greatest when the gates at the control structures were open. The ground-water flow model data were compared with the measured ground-water heads and vertical seepage from the wetlands. Estimating the horizontal ground-water flow rate beneath Levee 30 was difficult owing to the uncertainty in the horizontal hydraulic conductivity of the main flow zone of the Biscayne aquifer. Measurements of ground-water flows into Levee 30 canal, a substantial component of the water budget, were also uncertain, which lessened the ability to validate the model results. Because of vertical flows near Levee 30 canal and a very low hydraulic gradient east of the canal, a simplified Darcian approach simulated with the ground-water flow model does not accurately estimate the horizontal ground-water flow rate. Horizontal ground-water flow rates simulated with the ground-water flow model (for a 60-foot-deep by 1-foot-wide section of the Biscayne aquifer) ranged from 150 to 450 cubic feet per day west of Levee 30 and from 15 to 170 cubic feet per day east of Levee 30 canal. Vertical seepage from the wetlands, within 500 feet of Levee 30, generally accounted for 10 to 15 percent of the total horizontal flow beneath the levee. Simulated horizontal ground-water flow was highest during the wet season and when the gates at the control structures were open.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri014074","usgsCitation":"Sonenshein, R., 2001, Methods to quantify seepage beneath Levee 30, Miami-Dade County, Florida: U.S. Geological Survey Water-Resources Investigations Report 2001-4074, iv, 36 p., https://doi.org/10.3133/wri014074.","productDescription":"iv, 36 p.","costCenters":[],"links":[{"id":414247,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_42283.htm","linkFileType":{"id":5,"text":"html"}},{"id":160322,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2881,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri014074/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","county":"Miami-Dad County","otherGeospatial":"Levee 30","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -80.417,\n 25.95\n ],\n [\n -80.5,\n 25.95\n ],\n [\n -80.5,\n 25.758\n ],\n [\n -80.417,\n 25.758\n ],\n [\n -80.417,\n 25.95\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a55e4b07f02db62d22d","contributors":{"authors":[{"text":"Sonenshein, R.S.","contributorId":10415,"corporation":false,"usgs":true,"family":"Sonenshein","given":"R.S.","email":"","affiliations":[],"preferred":false,"id":204353,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":31279,"text":"ofr01155 - 2001 - Selected hydrologic and water-quality data for Kamas Valley and vicinity, Summit County, Utah, 1997-2000","interactions":[],"lastModifiedDate":"2017-04-11T09:49:47","indexId":"ofr01155","displayToPublicDate":"2001-10-01T00:00:00","publicationYear":"2001","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":"2001-155","title":"Selected hydrologic and water-quality data for Kamas Valley and vicinity, Summit County, Utah, 1997-2000","docAbstract":"This report contains hydrologic and water-quality data collected in the Kamas Valley vicinity during a study from 1997 to 2000. The study area is in Summit County in north-central Utah and is part of the Middle Rocky Mountains Physiographic Province described by Fenneman (1931). Data were collected in Kamas Valley between the Uinta Mountains on the east and the West Hills on the west, the upper Weber River area, the Samak area along Beaver Creek, the Woodland area, and the Indian Hollow area. These areas, where population growth and water demand are concentrated, encompass about 70 square miles and include the Weber River, Beaver Creek, and Provo River drainages. Surface water is the dominant hydrologic resource. The combined average flow from these three drainages is about 345,000 acre-feet per year. Ground water is present in the unconsolidated deposits in Kamas Valley, in stream alluvium along Beaver Creek and the upper Weber River, and in the consolidated rocks surrounding Kamas Valley.
","language":"English","publisher":"U.S.Geological Survey","publisherLocation":"Salt Lake City, UT","doi":"10.3133/ofr01155","collaboration":"Prepared in cooperation with the Utah Department Of Natural Resources, Division of Water Rights; Utah Department of Environmental Quality, Division of Water Quality; Weber Basin Water Conservancy District; Davis and Weber Counties Canal Company; and the Weber River Water Users Association","usgsCitation":"Haraden, P.L., Spangler, L., Brooks, L., and Stolp, B., 2001, Selected hydrologic and water-quality data for Kamas Valley and vicinity, Summit County, Utah, 1997-2000: U.S. Geological Survey Open-File Report 2001-155, Report: iv, 85 p.; 1 Plate: 18.92 x 26.04 inches, https://doi.org/10.3133/ofr01155.","productDescription":"Report: iv, 85 p.; 1 Plate: 18.92 x 26.04 inches","numberOfPages":"93","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":160188,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":339531,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2001/ofr01155/pdf/OFR01155.pdf"},{"id":2903,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr01155","linkFileType":{"id":5,"text":"html"}},{"id":258661,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2001/0155/plate-1.pdf","size":"3.70 MB","linkFileType":{"id":1,"text":"pdf"}}],"scale":"1","country":"United States","state":"Utah","county":"Summit County","otherGeospatial":"Kamas Valley","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a06e4b07f02db5f8c45","contributors":{"authors":[{"text":"Haraden, Peter L.","contributorId":60276,"corporation":false,"usgs":true,"family":"Haraden","given":"Peter","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":205563,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Spangler, L.E.","contributorId":54230,"corporation":false,"usgs":true,"family":"Spangler","given":"L.E.","email":"","affiliations":[],"preferred":false,"id":205562,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brooks, L.E.","contributorId":41852,"corporation":false,"usgs":true,"family":"Brooks","given":"L.E.","email":"","affiliations":[],"preferred":false,"id":205561,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Stolp, Bernard J. 0000-0003-3803-1497","orcid":"https://orcid.org/0000-0003-3803-1497","contributorId":71942,"corporation":false,"usgs":true,"family":"Stolp","given":"Bernard J.","affiliations":[],"preferred":false,"id":205564,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":24908,"text":"ofr00310 - 2001 - Concentrations and loads of cadmium, lead, and zinc measured on the ascending and descending limbs of the 1999 snowmelt-runoff hydrographs for nine water-quality stations, Coeur d'Alene River basin, Idaho","interactions":[],"lastModifiedDate":"2012-11-25T20:33:04","indexId":"ofr00310","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2001","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":"2000-310","title":"Concentrations and loads of cadmium, lead, and zinc measured on the ascending and descending limbs of the 1999 snowmelt-runoff hydrographs for nine water-quality stations, Coeur d'Alene River basin, Idaho","docAbstract":"The Remedial Investigation/Feasibility Study conducted by the U.S. Environmental Protection Agency within the Spokane River Basin of northern Idaho and eastern Washington included extensive data-collection activities to determine the nature and extent of trace-element contamination within the basin. The U.S. Geological Survey designed and implemented synoptic sampling of a high-flow runoff event at selected water-quality stations during the 1999 water year. The objective was to quantify spatial and temporal differences in constituent concentrations and loads over the ascending and descending limbs of a hydrograph depicting a high-flow runoff event. Discharge and water-quality data were collected during spring 1999 snowmelt runoff (May through early June) at nine water-quality stations, one on the North Fork Coeur d’Alene River and eight on the South Fork Coeur d’Alene River. The nine stations were sam- pled for whole-water recoverable and dissolved concentrations and loads of cadmium, lead, and zinc.\nThe concentrations and loads sampled during the 1999 snowmelt-runoff event represented near-normal conditions, not flood conditions, in that the recurrence interval for discharge near the hydrograph peak was about 2 years. The general trend among the nine stations was an inverse relation between discharge and dissolved concentrations of cadmium, lead, and zinc, and a direct relation between discharge and whole-water recoverable concentrations of these constituents. The smallest loads of dissolved and whole-water recoverable cadmium, lead, and zinc were measured at South Fork Coeur d’Alene River above Deadman Gulch; constituent concentrations at this site were some of the smallest among those sampled, and discharge was also relatively small. The largest loads of dissolved and whole-water recoverable cadmium, lead, and zinc were measured at South Fork Coeur d’Alene River at Pinehurst; constituent concentrations at this site were large and discharge was the second-largest of all the discharge measurements.\nHysteresis effects on concentrations and loads over the ascending and descending limbs of the snowmelt-runoff hydrograph were quite apparent, especially for whole-water recoverable constituents. Hysteresis is present when a property, such as constituent concentration or load, has different values for a given discharge over the ascending and descending limbs of a hydrograph. During this study, loads of whole-water recoverable constituents on the ascending limb were between 1.5 and 3.6 times larger than those mea- sured on the descending limb at nearly equal discharge. In contrast, dissolved constituents showed minimal hysteresis effects.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr00310","isbn":"0094-9140","collaboration":"Prepared in cooperation with U.S. Environmental Protection Agency","usgsCitation":"Woods, P.F., 2001, Concentrations and loads of cadmium, lead, and zinc measured on the ascending and descending limbs of the 1999 snowmelt-runoff hydrographs for nine water-quality stations, Coeur d'Alene River basin, Idaho: U.S. Geological Survey Open-File Report 2000-310, iv, 42 p., https://doi.org/10.3133/ofr00310.","productDescription":"iv, 42 p.","numberOfPages":"48","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":262320,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0310/report.pdf"},{"id":262321,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2000/0310/report-thumb.jpg"}],"scale":"100000","projection":"Albers Equal-Area","country":"United States","state":"Idaho","otherGeospatial":"Bunker Hill Superfund;South Fork","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.4998,47.3499 ], [ -116.4998,47.8014 ], [ -115.4985,47.8014 ], [ -115.4985,47.3499 ], [ -116.4998,47.3499 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db636041","contributors":{"authors":[{"text":"Woods, Paul F.","contributorId":82273,"corporation":false,"usgs":true,"family":"Woods","given":"Paul","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":192779,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28935,"text":"wri20004244 - 2001 - Analytical versus numerical estimates of water-level declines caused by pumping, and a case study of the Iao Aquifer, Maui, Hawaii","interactions":[],"lastModifiedDate":"2023-04-06T19:59:38.937721","indexId":"wri20004244","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2001","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":"2000-4244","title":"Analytical versus numerical estimates of water-level declines caused by pumping, and a case study of the Iao Aquifer, Maui, Hawaii","docAbstract":"Comparisons were made between model-calculated water levels from a one-dimensional analytical model referred to as RAM (Robust Analytical Model) and those from numerical ground-water flow models using a sharp-interface model code. RAM incorporates the horizontal-flow assumption and the Ghyben-Herzberg relation to represent flow in a one-dimensional unconfined aquifer that contains a body of freshwater floating on denser saltwater. RAM does not account for the presence of a low-permeability coastal confining unit (caprock), which impedes the discharge of fresh ground water from the aquifer to the ocean, nor for the spatial distribution of ground-water withdrawals from wells, which is significant because water-level declines are greatest in the vicinity of withdrawal wells. Numerical ground-water flow models can readily account for discharge through a coastal confining unit and for the spatial distribution of ground-water withdrawals from wells.\r\n\r\nFor a given aquifer hydraulic-conductivity value, recharge rate, and withdrawal rate, model-calculated steady-state water-level declines from RAM can be significantly less than those from numerical ground-water flow models. The differences between model-calculated water-level declines from RAM and those from numerical models are partly dependent on the hydraulic properties of the aquifer system and the spatial distribution of ground-water withdrawals from wells. RAM invariably predicts the greatest water-level declines at the inland extent of the aquifer where the freshwater body is thickest and the potential for saltwater intrusion is lowest. For cases in which a low-permeability confining unit overlies the aquifer near the coast, however, water-level declines calculated from numerical models may exceed those from RAM even at the inland extent of the aquifer.\r\n\r\nSince 1990, RAM has been used by the State of Hawaii Commission on Water Resource Management for establishing sustainable-yield values for the State?s aquifers. Data from the Iao aquifer, which lies on the northeastern flank of the West Maui Volcano and which is confined near the coast by caprock, are now available to evaluate the predictive capability of RAM for this system. In 1995 and 1996, withdrawal from the Iao aquifer reached the 20 million gallon per day sustainable-yield value derived using RAM. However, even before 1996, water levels in the aquifer had declined significantly below those predicted by RAM, and continued to decline in 1997. To halt the decline of water levels and to preclude the intrusion of salt-water into the four major well fields in the aquifer, it was necessary to reduce withdrawal from the aquifer system below the sustainable-yield value derived using RAM. \r\n\r\nIn the Iao aquifer, the decline of measured water levels below those predicted by RAM is consistent with the results of the numerical model analysis. Relative to model-calculated water-level declines from numerical ground-water flow models, (1) RAM underestimates water-level declines in areas where a low-permeability confining unit exists, and (2) RAM underestimates water-level declines in the vicinity of withdrawal wells.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri20004244","usgsCitation":"Oki, D.S., and Meyer, W., 2001, Analytical versus numerical estimates of water-level declines caused by pumping, and a case study of the Iao Aquifer, Maui, Hawaii: U.S. Geological Survey Water-Resources Investigations Report 2000-4244, iv, 31 p., https://doi.org/10.3133/wri20004244.","productDescription":"iv, 31 p.","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":124608,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_2000_4244.jpg"},{"id":415376,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34827.htm","linkFileType":{"id":5,"text":"html"}},{"id":13744,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri00-4244/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Iao aquifer, Maui","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.598,\n 20.94\n ],\n [\n -156.598,\n 20.838\n ],\n [\n -156.465,\n 20.838\n ],\n [\n -156.465,\n 20.94\n ],\n [\n -156.598,\n 20.94\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e459","contributors":{"authors":[{"text":"Oki, Delwyn S. 0000-0002-6913-8804 dsoki@usgs.gov","orcid":"https://orcid.org/0000-0002-6913-8804","contributorId":1901,"corporation":false,"usgs":true,"family":"Oki","given":"Delwyn","email":"dsoki@usgs.gov","middleInitial":"S.","affiliations":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200644,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Meyer, William","contributorId":87538,"corporation":false,"usgs":true,"family":"Meyer","given":"William","affiliations":[],"preferred":false,"id":200645,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30905,"text":"wri014040 - 2001 - Pond-aquifer interaction at South Pond of Lake Cochituate, Natick, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:09:07","indexId":"wri014040","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2001","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":"2001-4040","title":"Pond-aquifer interaction at South Pond of Lake Cochituate, Natick, Massachusetts","docAbstract":"A U.S. Army facility on a peninsula in South Pond of Lake Cochituate was designated a Superfund site by the U.S. Environmental Protection Agency in 1994 because contaminated ground water was detected at the facility, which is near the Natick Springvale public-supply wellfield. The interaction between South Pond and the underlying aquifer controls ground-water flow patterns near the pond and determines the source of water withdrawn from the wellfield.A map of the bathymetry and the thickness of fine-grained pond-bottom sediments was prepared on the basis of fathometer, ground-penetrating radar, and continuous seismic-reflection surveys. The geophysical data indicate that the bottom sediments are fine grained toward the middle of the pond but are coarse grained in shoreline areas. Natick Springvale wellfield, which consists of three active public-supply wells adjacent to South Pond, is 2,200 feet downgradient from the boundary of the Army facility. That part of South Pond between the Natick Springvale wellfield and the Army facility is 18 feet deep with at least 14 feet of fine-grained sediment beneath the pond-bottom. Water levels from the pond and underlying sediments indicate a downward vertical gradient and the potential for infiltration of pond water near the wellfield. Head differences between the pond and the wellfield ranged from 1.66 to 4.41 feet during this study. The velocity of downward flow from South Pond into the pond-bottom sediments, determined on the basis of temperature profiles measured over a diurnal cycle at two locations near the wellfield, was 0.5 and 1.0 feet per day. These downward velocities resulted in vertical hydraulic conductivities of 1.1 and 2.9 feet per day for the pond-bottom sediments.Naturally occurring stable isotopes of oxygen and hydrogen were used as tracers of pond water and ground water derived from recharge of precipitation, two potential sources of water to a well in a pond-aquifer setting. The isotopic composition of pond water varied seasonally and was distinctly different from the isotopic composition of ground water. The isotopic composition of shallow water beneath and adjacent to South Pond near the wellfield corresponds to the temporal variation of pond water, indicating that nearly all water at shallow depths was derived from pond water. A two-component mixing model based on the average stable isotope values of the source waters indicated that 64 ?15 percent at the 95-percent confidence interval of the water withdrawn at the public-supply wells was derived from the pond; pond water accounted for most of the uncertainty in the result. The rate of infiltration of pond water into the aquifer and discharging to the wellfield was 1.0 million gallons per day at the average pumping rate.","language":"ENGLISH","doi":"10.3133/wri014040","usgsCitation":"Friesz, P.J., and Church, P.E., 2001, Pond-aquifer interaction at South Pond of Lake Cochituate, Natick, Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 2001-4040, 42 p., 1 over-size sheet. , https://doi.org/10.3133/wri014040.","productDescription":"42 p., 1 over-size sheet. ","costCenters":[],"links":[{"id":2840,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri014040","linkFileType":{"id":5,"text":"html"}},{"id":160730,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db68437a","contributors":{"authors":[{"text":"Friesz, Paul J. 0000-0002-4660-2336 pfriesz@usgs.gov","orcid":"https://orcid.org/0000-0002-4660-2336","contributorId":1075,"corporation":false,"usgs":true,"family":"Friesz","given":"Paul","email":"pfriesz@usgs.gov","middleInitial":"J.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204327,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Church, Peter E.","contributorId":99178,"corporation":false,"usgs":true,"family":"Church","given":"Peter","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":204328,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30898,"text":"wri014015 - 2001 - Hydrogeologic framework and geochemistry of the intermediate aquifer system in parts of Charlotte, De Soto, and Sarasota counties, Florida","interactions":[],"lastModifiedDate":"2012-02-02T00:08:59","indexId":"wri014015","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2001","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":"2001-4015","title":"Hydrogeologic framework and geochemistry of the intermediate aquifer system in parts of Charlotte, De Soto, and Sarasota counties, Florida","docAbstract":"The hydrogeologic framework underlying the 600-square-mile study area in Charlotte, De Soto, and Sarasota Counties, Florida, consists of the surficial aquifer system, the intermediate aquifer system, and the Upper Floridan aquifer. The hydrogeologic framework and the geochemical processes controlling ground-water composition were evaluated for the study area. Particular emphasis was given to the analysis of hydrogeologic and geochemical data for the intermediate aquifer system. Flow regimes are not well understood in the intermediate aquifer system; therefore, hydrogeologic and geochemical information were used to evaluate connections between permeable zones within the intermediate aquifer system and between overlying and underlying aquifer systems. Knowledge of these connections will ultimately help to protect ground-water quality in the intermediate aquifer system. The hydrogeology was interpreted from lithologic and geophysical logs, water levels, hydraulic properties, and water quality from six separate well sites. Water-quality samples were collected from wells located along six ground-water flow paths and finished at different depth intervals. The selection of flow paths was based on current potentiometric-surface maps. Ground-water samples were analyzed for major ions; field parameters (temperature, pH, specific conductance, and alkalinity); stable isotopes (deuterium, oxygen-18, and carbon-13); and radioactive isotopes (tritium and carbon-14). The surficial aquifer system is the uppermost aquifer, is unconfined, relatively thin, and consists of unconsolidated sand, shell, and limestone. The intermediate aquifer system underlies the surficial aquifer system and is composed of clastic sediments interbedded with carbonate rocks. The intermediate aquifer system is divided into three permeable zones, the Tamiami/Peace River zone (PZ1), the Upper Arcadia zone (PZ2), and the Lower Arcadia zone (PZ3). The Tamiami/Peace River zone (PZ1) is the uppermost zone and is the thinnest and generally, the least productive zone in the intermediate aquifer system. The Upper Arcadia zone (PZ2) is the middle zone and productivity is generally higher than the overlying permeable zone. The Lower Arcadia zone (PZ3) is the lowermost permeable zone and is the most productive zone in the intermediate aquifer system. The intermediate aquifer system is underlain by the Upper Floridan aquifer, which consists of a thick, stratified sequence of limestone and dolomite. The Upper Floridan aquifer is the most productive aquifer in the study area; however, its use is generally restricted because of poor water quality. Interbedded clays and fine-grained clastics separate the aquifer systems and permeable zones. The hydraulic properties of the three aquifer systems are spatially variable. Estimated trans-missivity and horizontal hydraulic conductivity varies from 752 to 32,900 feet squared per day and from 33 to 1,490 feet per day, respectively, for the surficial aquifer system; from 47 to 5,420 feet squared per day and from 2 to 102 feet per day, respectively, for the Tamiami/Peace River zone (PZ1); from 258 to 24,633 feet squared per day and from 2 to 14 feet per day, respectively, for the Upper Arcadia zone (PZ2); from 766 to 44,900 feet squared per day and from 10 to 201 feet per day, respectively, for the Lower Arcadia zone (PZ3); and from 2,350 to 7,640 feet squared per day and from 10 to 41 feet per day, respectively, for the Upper Floridan aquifer. Confining units separating the aquifer systems have leakance coefficients estimated to range from 2.3 x 10-5 to 5.6 x 10-3 feet per day per foot. Strata composing the confining unit separating the Upper Floridan aquifer from the intermediate aquifer system are substantially more permeable than confining units separating the permeable zones in the intermediate aquifer system or separating the surficial aquifer and intermediate aquifer systems. In Charlotte, Sarasota, and western De Soto Counties, hydraulic","language":"ENGLISH","doi":"10.3133/wri014015","usgsCitation":"Torres, A.E., Sacks, L.A., Yobbi, D.K., Knochenmus, L.A., and Katz, B., 2001, Hydrogeologic framework and geochemistry of the intermediate aquifer system in parts of Charlotte, De Soto, and Sarasota counties, Florida: U.S. Geological Survey Water-Resources Investigations Report 2001-4015, 74 p. , https://doi.org/10.3133/wri014015.","productDescription":"74 p. ","costCenters":[],"links":[{"id":2836,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri014015/","linkFileType":{"id":5,"text":"html"}},{"id":160129,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696bf0","contributors":{"authors":[{"text":"Torres, A. E.","contributorId":94350,"corporation":false,"usgs":true,"family":"Torres","given":"A.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":204312,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sacks, L. A.","contributorId":83092,"corporation":false,"usgs":true,"family":"Sacks","given":"L.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":204311,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Yobbi, D. K.","contributorId":56622,"corporation":false,"usgs":true,"family":"Yobbi","given":"D.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":204308,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Knochenmus, L. A.","contributorId":60683,"corporation":false,"usgs":true,"family":"Knochenmus","given":"L.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":204309,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Katz, B. G.","contributorId":82702,"corporation":false,"usgs":true,"family":"Katz","given":"B. G.","affiliations":[],"preferred":false,"id":204310,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":30897,"text":"wri014014 - 2001 - Analysis of borehole-radar reflection logs from selected HC boreholes at the Project Shoal area, Churchill County, Nevada","interactions":[],"lastModifiedDate":"2019-10-15T11:28:55","indexId":"wri014014","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2001","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":"2001-4014","title":"Analysis of borehole-radar reflection logs from selected HC boreholes at the Project Shoal area, Churchill County, Nevada","docAbstract":"Single-hole borehole-radar reflection logs were collected and interpreted in support of a study to characterize ground-water flow and transport at the Project Shoal Area (PSA) in Churchill County, Nevada. Radar logging was conducted in six boreholes using 60-MHz omni-directional electric-dipole antennas and a 60-MHz magnetic-dipole directional receiving antenna.Radar data from five boreholes were interpreted to identify the location, orientation, estimated length, and spatial continuity of planar reflectors present in the logs. The overall quality of the radar data is marginal and ranges from very poor to good. Twenty-seven reflectors were interpreted from the directional radar reflection logs. Although the range of orientation interpreted for the reflectors is large, a significant number of reflectors strike northeast-southwest and east-west to slightly northwest-southeast. Reflectors are moderate to steeply dipping and reflector length ranged from less than 7 m to more than 133 m.Qualitative scores were assigned to each reflector to provide a sense of the spatial continuity of the reflector and the characteristics of the field data relative to an ideal planar reflector (orientation score). The overall orientation scores are low, which reflects the general data quality, but also indicates that the properties of most reflectors depart from the ideal planar case. The low scores are consistent with reflections from fracture zones that contain numerous, closely spaced, sub-parallel fractures.Interpretation of borehole-radar direct-wave velocity and amplitude logs identified several characteristics of the logged boreholes: (1) low-velocity zones correlate with decreased direct-wave amplitude, indicating the presence of fracture zones; (2) direct-wave amplitude increases with depth in three of the boreholes, suggesting an increase in electrical resistivity with depth resulting from changes in mineral assemblage or from a decrease in the specific conductance of ground water; and (3) an increase in primary or secondary porosity and an associated change in mineral assemblage, or decrease in ground water specific conductance, was characterized in two of the boreholes below 300 m.The results of the radar reflection logging indicate that even where data quality is marginal, borehole-radar reflection logging can provide useful information for ground-water characterization studies in fractured rock and insights into the nature and extent of fractures and fracture zones in and near boreholes.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri014014","usgsCitation":"Lane, J., Joesten, P., Pohll, G., and Mihevic, T., 2001, Analysis of borehole-radar reflection logs from selected HC boreholes at the Project Shoal area, Churchill County, Nevada: U.S. Geological Survey Water-Resources Investigations Report 2001-4014, iv, 23 p. , https://doi.org/10.3133/wri014014.","productDescription":"iv, 23 p. 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J.W. Jr.","contributorId":66723,"corporation":false,"usgs":true,"family":"Lane","given":"J.W.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":204306,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Joesten, P. K.","contributorId":62818,"corporation":false,"usgs":true,"family":"Joesten","given":"P. K.","affiliations":[],"preferred":false,"id":204304,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pohll, G.M.","contributorId":65261,"corporation":false,"usgs":true,"family":"Pohll","given":"G.M.","email":"","affiliations":[],"preferred":false,"id":204305,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mihevic, Todd","contributorId":87416,"corporation":false,"usgs":true,"family":"Mihevic","given":"Todd","email":"","affiliations":[],"preferred":false,"id":204307,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":30858,"text":"wri004061 - 2001 - Nutrients and organic compounds in Deer Creek and south branch Plum Creek in southwestern Pennsylvania, April 1996 through September 1998","interactions":[],"lastModifiedDate":"2025-01-13T22:00:41.597288","indexId":"wri004061","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2001","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":"2000-4061","title":"Nutrients and organic compounds in Deer Creek and south branch Plum Creek in southwestern Pennsylvania, April 1996 through September 1998","docAbstract":"This report presents results of an analysis of nutrient and pesticide data from two surface-water sites and volatile organic compound (VOC) data from one of the sites that are within the Allegheny and Monongahela River Basins study unit of the National Water-Quality Assessment Program of the U.S. Geological Survey. The Deer Creek site was located in a 27.0 square-mile basin within the Allegheny River Basin in Allegheny County. The primary land uses consist of small urban areas, large areas of residential housing, and some agricultural land in the upper part of the basin. The South Branch Plum Creek site was located in a 33.3 square-mile basin within the Allegheny River Basin in Indiana County. The primary land uses throughout this basin are mostly agriculture and forestland.
Water samples for analysis of nutrients were collected monthly and during high-flow events from April 1996 through September 1998. Concentrations of dissolved nitrite, dissolved ammonia plus organic nitrogen, and dissolved phosphorus were less than the method detection limits in more than one-half of the samples collected. The median concentration of dissolved nitrite plus nitrate in South Branch Plum Creek was 0.937 mg/L and 0.597 mg/L in Deer Creek. The median concentration of dissolved orthophosphate was 0.01 mg/L in both streams. High loads of nitrate were measured in both streams from March to June. Concentrations of dissolved ammonia nitrogen, dissolved nitrate, and total phosphorus were lower during the summer months. Measured concentrations of nitrate nitrogen in both streams were well below the U.S. Environmental Protection Agency (USEPA) maximum contaminant level (MCL) of 10 mg/L.
Water samples for analysis of pesticides were collected throughout 1997 in both streams and during a storm event on August 25-26, 1998, in Deer Creek. Samples were collected monthly at both sites and more frequently during the spring and early summer months to coincide with application of pesticides. Seventy-eight pesticides and 7 pesticide metabolites were analyzed in 31 samples collected in Deer Creek and in 18 samples collected in South Branch Plum Creek. Of the 85 pesticides and pesticide metabolites analyzed, 25 of the pesticides were detected at least once in Deer Creek, and 20 of the pesticides were detected at least once in South Branch Plum Creek. Atrazine was the most commonly detected pesticide in both streams. There was a distinct seasonal pattern of atrazine, simazine, and metolachlor concentrations measured at both sites.
Prometon was detected in 3 of the 18 samples collected in South Branch Plum Creek in 1997 and in 28 of the 31 samples collected in Deer Creek in both 1997 and 1998. Prometon generally is applied in conjunction with asphalt paving projects and is commonly used in residential areas. The highest measured concentrations of prometon detected in Deer Creek were in the five storm samples collected on August 25-26, 1998.
At the Deer Creek site, 9 of the 25 pesticides detected throughout the study were detected only in the sample collected on June 13, 1997. Those nine pesticides included acifluorfen, bentazon, bromoxynil, dicamba, dichlorprop, fenuron, linuron, MCPA, and neburon. Nine other pesticides also were detected in that sample.
All concentrations of pesticides were well below established drinking-water guidelines. The maximum measured concentration of diazinon in Deer Creek (0.097 µg/L) and South Branch Plum Creek (0.974 µg/L) exceeded the aquatic life guideline of 0.009 µg/L established by the National Academy of Sciences/National Academy of Engineers. The maximum measured concentration of azinphos-methyl in South Branch Plum Creek (an estimated value of 0.033 µg/L) exceeded the chronic aquatic-life guideline of 0.01 µg/L established by the USEPA.
Twenty-five samples were collected from Deer Creek and analyzed for volatile organic compounds (VOCs). Of 87 VOCs analyzed for, 22 were detected at least once, and 12 were gasoline-related compounds. Acetone, benzene, carbon disulfide, meta/paraxylene, methyl chloride, MTBE, p-isopropyl toluene, toluene, and 1,2,4-trimethylbenzene were each detected in five or more samples. VOCs generally were detected during the colder winter months and not frequently during the summer months.
The maximum measured concentrations of benzene, ethylbenzene, o-dichlorobenzene, styrene, and toluene were two or more orders of magnitude lower than the MCLs established by the USEPA.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004061","usgsCitation":"Williams, D., and Clark, M., 2001, Nutrients and organic compounds in Deer Creek and south branch Plum Creek in southwestern Pennsylvania, April 1996 through September 1998: U.S. Geological Survey Water-Resources Investigations Report 2000-4061, viii, 47 p., https://doi.org/10.3133/wri004061.","productDescription":"viii, 47 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":119291,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4061/coverthb.jpg"},{"id":466173,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_39864.htm","text":"Deer Creek basin","linkFileType":{"id":5,"text":"html"}},{"id":466174,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_39865.htm","text":"South Branch Plum Creek basin","linkFileType":{"id":5,"text":"html"}},{"id":2736,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4061/wri20004061.pdf","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2000-4061"}],"country":"United States","state":"Pennsylvania","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.419921875,\n 38.634036452919226\n ],\n [\n -77.84912109375,\n 38.634036452919226\n ],\n [\n -77.84912109375,\n 41.9921602333763\n ],\n [\n -80.419921875,\n 41.9921602333763\n ],\n [\n -80.419921875,\n 38.634036452919226\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
Pennsylvania Water Science Center
215 Limekiln Road
New Cumberland, PA 17070
The Hudson River is being considered for use as a supplemental source of water supply for New York City during droughts. One proposal entails withdrawal of Hudson River water from locations near Newburgh, Chelsea, or Kingston, but the extent to which this could cause the salt front to advance upstream to points where it could adversely affect community water supplies is unknown. The U.S. Geological Survey (USGS) one-dimensional Branch-Network Dynamic Flow model (BRANCH) was used in conjunction with the USGS one-dimensional Branched Lagrangian Solute-Transport Model (BLTM) to simulate the effect of five water-withdrawal scenarios on the salt-front location.
The modeled reach contains 132 miles of the lower Hudson River between the Federal Dam at Troy and Hastings-on-Hudson (near New York City). The BRANCH model was calibrated and verified to 19 tidal-cycle discharge measurements made at 11 locations by conventional and acoustic Doppler current-profiler methods. Maximum measured instantaneous tidal flow ranged from 20,000 ft3/s (cubic feet per second) at Albany to 368,000 ft3/s at Tellers Point; daily-mean flow at Green Island near Troy ranged from 3,030 ft3/s to 45,000 ft3/s during the flow measurements. Successive ebb- and flood-flow volumes were measured and compared with computed volumes; daily-mean bias was -1.6 percent (range from -21.0 to +23.7 percent; 13.5 percent mean absolute error). Daily-mean deviation between simulated and measured stage at eight locations (from Bowline Point to Albany) over the 19 tidal-cycle measurements averaged +0.06 ft (range from -0.31 to +0.40 ft; 0.21 ft root mean square error, RMSE). These results indicate that the model can accurately simulate flow in the Hudson River under a wide range of flow, tide, and meteorological conditions.
The BLTM was used to simulate chloride transport in the 61-mi reach from Turkey Point to Bowline Point under two seasonal conditions in 1990.one representing spring conditions of high inflow and low salinity (April-June), the other representing typical summer conditions of low inflow and high salinity (July-August). Measured chloride concentrations at Bowline Point were used to drive the BLTM simulations, and data collected at West Point were used for calibration. Mean bias in simulated chloride concentration for the April-June 1990 (high flow) data (observed range from 12 to 201 mg/L [milligrams per liter]; 30 mg/L RMSE) was .16 mg/L, and mean bias for the July-August 1990 (low flow) data (observed range from 31 to 2,000 mg/L; 535 mg/ L RMSE) was +126 mg/L. The salt front (saltwater/ freshwater interface) on the Hudson River was defined as the furthest upstream location where the chloride concentration exceeded 100 mg/L. Data from August 1991 were used to evaluate solute transport between West Point and Poughkeepsie because a chloride concentration of 100 mg/L was not observed at Clinton Point in 1990. The BLTM then was used to simulate chloride concentrations at Chelsea Pump Station and Clinton Point. Regression equations, based on daily mean values of specific conductance measured at West Point, were used to estimate daily mean chloride concentrations at Chelsea Pump Station and Clinton Point for model analysis. Mean biases in BLTM-simulated daily mean chloride concentrations for August 1991 were .38 mg/L at Chelsea Pump Station (range from 189 to 551 mg/L; 103 mg/L RMSE) and .9 mg/L at Clinton Point (range from 53 to 264 mg/L; 62 mg/L RMSE).
Hypothetical withdrawals at (1) Newburgh, (2) Chelsea, (3) Chelsea and Newburgh, (4) Chelsea and Kingston, and (5) Kingston and Newburgh, were simulated to compute the effects of withdrawals on salt-front movement. Withdrawals of 300 Mgal/d from any combination of Chelsea or Newburgh could result in upstream movement of the salt front of as much as 1.0 mi, given an initial salt-front location between West Point and Rogers Point. Scenarios that included withdrawals at Kingston caused the greatest upstream salt-front movement. Simulation of a 90-day April-June high-flow period during which discharges at Green Island averaged 25,200 ft3/s indicated that withdrawals of 1,939 Mgal/d (million gallons per day) at Chelsea Pump Station would not measureably increase chloride concentrations at Chelsea Pump Station under normal tidal and meteorological conditions, but withdrawals at twice that rate (3,878 Mgal/d) could increase the chloride concentration at Chelsea Pump Station to 250 mg/L.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri994024","collaboration":"Prepared in cooperation with the New York City Department of Environmental ProtectionDirector, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
Suspended sediment has long been recognized as an important contaminant affecting water resources. Besides its direct role in determining water clarity, bridge scour and reservoir storage, sediment serves as a vehicle for the transport of many binding contaminants, including nutrients, trace metals, semi-volatile organic compounds, a nd numerous pesticides (U.S. Environmental Protection Agency, 2000a). Recent efforts to addr ess water-quality concerns through the Total Maximum Daily Load (TMDL) process have iden tified sediment as the single most prevalent cause of impairment in the Nation’s streams a nd rivers (U.S. Environmental Protection Agency, 2000b). Moreover, sediment has been identified as a medium for the tran sport and sequestration of organic carbon, playing a potentia lly important role in understa nding sources and sinks in the global carbon budget (Stallard, 1998).
A comprehensive understanding of sediment fate a nd transport is considered essential to the design and implementation of effective plans for sediment management (Osterkamp and others, 1998, U.S. General Accounting Office, 1990). An exte nsive literature addr essing the problem of quantifying sediment transport has produced a nu mber of methods for estimating its flux (see Cohn, 1995, and Robertson and Roerish, 1999, for us eful surveys). The accuracy of these methods is compromised by uncertainty in the concentration measurements and by the highly episodic nature of sediment movement, particul arly when the methods are applied to smaller basins. However, for annual or decadal flux es timates, the methods are generally reliable if calibrated with extended periods of data (Robertson and Roerish, 1999). A substantial literature also supports the Universal Soil Loss Equation (U SLE) (Soil Conservation Service, 1983), an engineering method for estimating sheet and rill erosion, although the empirical credentials of the USLE have recently been questioned (Tri mble and Crosson, 2000). Conversely, relatively little direct evidence is available concerning the fate of sediment. The common practice of quantifying sediment fate with a sediment deliv ery ratio, estimated from a simple empirical relation with upstream basin area, does not artic ulate the relative importance of individual storage sites within a basin (Wolman, 1977). Rates of sediment deposition in reservoirs and flood plains can be determined from empirical measurement s , but only a limited number of sites have been monitored, and net rates of deposition or loss from other potential sinks and sources is largely unknown (Stallard, 1998). In particular, little is known about how much sediment loss from fields ultimately makes its way to stream channels, and how much sediment is subsequently stored in or lost from th e streambed (Meade and Parker, 1985, Trimble and Crosson, 2000).
This paper reports on recent progress made to a ddress empirically the question of sediment fate and transport on a national scale. The model pres ented here is based on the SPAtially Referenced Regression On Watershed attr ibutes (SPARROW) methodology, fi rst used to estimate the distribution of nutrients in str eams and rivers of the United Stat es, and subsequently shown to describe land and stream processes affecting the delivery of nutrients (Smith and others, 1997, Alexander and others, 2000, Preston and Brakeb ill, 1999). The model makes use of numerous spatial datasets, available at the national level, to explain long-term sediment water-quality conditions in major streams and rivers throughou t the United States. Sediment sources are identified using sediment erosion rates from the National Resources I nventory (NRI) (Natural Resources Conservation Service, 2000) and apportioned over the landscape according to 30- meter resolution land-use information from th e National Land Cover Data set (NLCD) (U.S. Geological Survey, 2000a). More than 76,000 reservoirs from the National Inventory of Dams (NID) (U.S. Army Corps of Engin eers, 1996) are identified as pot ential sediment sinks. Other, non-anthropogenic sources and sinks are identified using soil in formation from the State Soil Survey Geographic (STATSGO) data base (Schwarz and Alexander, 1995) and spatial coverages representing surficial rock t ype and vegetative cover. The SPA RROW model empirically relates these diverse spatial datasets to estimates of long-term, mean annual sediment flux computed from concentration and flow measurements co llected over the period 1985 -95 from more than 400 monitoring stations maintained by the Na tional Stream Quality Accounting Network (Alexander and others, 1998), the National Wa ter Quality Assessment Program, and U.S. Geological Survey District offices (Turcios and Gray, in press). Th e calibrated model is used to estimate sediment flux for over 60,000 stream segments included in the River Reach File 1 (RF1) stream network (Alexander and others, 1999).
SPARROW uses statis tical methods to calibrate a simple, structural model of riverine water quality, one that imposes mass ba lance in accounting for changes in contaminant flux. As applied here, the mass-balance approach facilitates the interpretation of model results in terms of physical processes affecting sediment transport, and makes possible the estimation of various rates of sediment generation and loss associated with stream channels and features of the landscape. The statistical approach provides a basi s for assessing the error of these inferred rates and of the error in extrapolated estimates of sediment flux made for streams in the RF1 network. An important implication of the holistic modeling approach adopted in this analysis is that estimates of sediment production and loss ar e based on, and therefore consistent with, measurements of in-stream flux. Other ancillary information, such as direct measurements of long-term sediment storage and release from rese rvoirs (Steffen, 1996), is incorporated into the analysis by specifying additional equations expl aining these ancillary variables. The imposition of cross-equation constraints affords this info rmation a statistically consistent weight in explaining in-stream sediment flux. Thus, the me thodology described here represents a general framework for synthesizing a wide spectrum of available information relevant to the understanding of sediment fate and transport.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Proceedings of the Seventh Federal Interagency Sedimentation Conference, March 25 to 29, 2001, Reno, Nevada","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"7th Federal Interagency Sedimentation Conference","conferenceDate":"Mar 25-29, 2001","conferenceLocation":"Reno, NV","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","usgsCitation":"Schwarz, G., Smith, R.A., Alexander, R.B., and Gray, J.R., 2001, A spatially referenced regression model (SPARROW) for suspended sediment in streams of the Conterminous U.S., in Proceedings of the Seventh Federal Interagency Sedimentation Conference, March 25 to 29, 2001, Reno, Nevada, v. II, Reno, NV, Mar 25-29, 2001, p. VII-80-VII-87.","productDescription":"8 p.","startPage":"VII-80","endPage":"VII-87","costCenters":[{"id":502,"text":"Office of Surface Water","active":true,"usgs":true}],"links":[{"id":292269,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Conterminous United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"geometry\": {\n \"type\": \"MultiPolygon\",\n \"coordinates\": [\n [\n [\n [\n -94.81758,\n 49.38905\n ],\n [\n -94.64,\n 48.84\n ],\n [\n -94.32914,\n 48.67074\n ],\n [\n -93.63087,\n 48.60926\n ],\n [\n -92.61,\n 48.45\n ],\n [\n -91.64,\n 48.14\n ],\n [\n -90.83,\n 48.27\n ],\n [\n -89.6,\n 48.01\n ],\n [\n -89.27292,\n 48.01981\n ],\n [\n -88.37811,\n 48.30292\n ],\n [\n -87.43979,\n 47.94\n ],\n [\n -86.46199,\n 47.55334\n ],\n [\n -85.65236,\n 47.22022\n ],\n [\n -84.87608,\n 46.90008\n ],\n [\n -84.77924,\n 46.6371\n 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]\n}","volume":"II","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ef1ec1e4b0bfa1f993eece","contributors":{"authors":[{"text":"Schwarz, Gregory E. 0000-0002-9239-4566 gschwarz@usgs.gov","orcid":"https://orcid.org/0000-0002-9239-4566","contributorId":543,"corporation":false,"usgs":true,"family":"Schwarz","given":"Gregory E.","email":"gschwarz@usgs.gov","affiliations":[{"id":5067,"text":"Northeast Regional Director's Office","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":false,"id":498327,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, Richard A. 0000-0003-2117-2269 rsmith1@usgs.gov","orcid":"https://orcid.org/0000-0003-2117-2269","contributorId":580,"corporation":false,"usgs":true,"family":"Smith","given":"Richard","email":"rsmith1@usgs.gov","middleInitial":"A.","affiliations":[{"id":503,"text":"Office of Water Quality","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true},{"id":37778,"text":"WMA - Integrated Modeling and Prediction Division","active":true,"usgs":true}],"preferred":true,"id":498328,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Alexander, Richard B. 0000-0001-9166-0626 ralex@usgs.gov","orcid":"https://orcid.org/0000-0001-9166-0626","contributorId":541,"corporation":false,"usgs":true,"family":"Alexander","given":"Richard","email":"ralex@usgs.gov","middleInitial":"B.","affiliations":[{"id":503,"text":"Office of Water Quality","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true}],"preferred":true,"id":498326,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Gray, John R. 0000-0002-8817-3701 jrgray@usgs.gov","orcid":"https://orcid.org/0000-0002-8817-3701","contributorId":1158,"corporation":false,"usgs":true,"family":"Gray","given":"John","email":"jrgray@usgs.gov","middleInitial":"R.","affiliations":[{"id":5058,"text":"Office of the Chief Scientist for Water","active":true,"usgs":true}],"preferred":true,"id":498329,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":32924,"text":"pp1642 - 2001 - Geochronology and geology of late Oligocene through Miocene volcanism and mineralization in the western San Juan Mountains, Colorado","interactions":[],"lastModifiedDate":"2018-11-19T11:18:00","indexId":"pp1642","displayToPublicDate":"2001-08-01T00:00:00","publicationYear":"2001","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1642","title":"Geochronology and geology of late Oligocene through Miocene volcanism and mineralization in the western San Juan Mountains, Colorado","docAbstract":"This paper presents 25 new 40Ar/39Ar dates from the main calc-alkaline ash-flow sheets and related younger plutons of the western San Juan volcanic field, the ash-flow sheets of the Lake City caldera cycle, and veins and other altered rocks in the Lake City region. The goal of the study was to produce similar quality 40Ar/39Ar ages to those currently published for the eastern and central San Juan Mountains. These new data provide a much more precise chronological framework for interpreting durations of events and their relationship to mineralization than do previously published conventional K-Ar dates for the western San Juan Mountains.","language":"ENGLISH","doi":"10.3133/pp1642","usgsCitation":"Bove, D.J., Hon, K., Budding, K.E., Slack, J.F., Snee, L., and Yeoman, R.A., 2001, Geochronology and geology of late Oligocene through Miocene volcanism and mineralization in the western San Juan Mountains, Colorado: U.S. Geological Survey Professional Paper 1642, 30 p., https://doi.org/10.3133/pp1642.","productDescription":"30 p.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":119357,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1642/report-thumb.jpg"},{"id":60840,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1642/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b1e4b07f02db530747","contributors":{"authors":[{"text":"Bove, Dana J. dbove@usgs.gov","contributorId":4855,"corporation":false,"usgs":true,"family":"Bove","given":"Dana","email":"dbove@usgs.gov","middleInitial":"J.","affiliations":[],"preferred":true,"id":209434,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hon, Ken","contributorId":19163,"corporation":false,"usgs":true,"family":"Hon","given":"Ken","affiliations":[],"preferred":false,"id":209435,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Budding, Karin E.","contributorId":32164,"corporation":false,"usgs":true,"family":"Budding","given":"Karin","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":209436,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Slack, John F. 0000-0001-6600-3130 jfslack@usgs.gov","orcid":"https://orcid.org/0000-0001-6600-3130","contributorId":1032,"corporation":false,"usgs":true,"family":"Slack","given":"John","email":"jfslack@usgs.gov","middleInitial":"F.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":209433,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Snee, Lawrence W.","contributorId":81534,"corporation":false,"usgs":true,"family":"Snee","given":"Lawrence W.","affiliations":[],"preferred":false,"id":209437,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Yeoman, Ross A.","contributorId":93107,"corporation":false,"usgs":true,"family":"Yeoman","given":"Ross","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":209438,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":30877,"text":"wri004231 - 2001 - Effects of remedial grouting on the ground-water flow system at Red Rock Dam near Pella, Iowa","interactions":[],"lastModifiedDate":"2016-02-08T13:17:50","indexId":"wri004231","displayToPublicDate":"2001-08-01T00:00:00","publicationYear":"2001","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":"2000-4231","title":"Effects of remedial grouting on the ground-water flow system at Red Rock Dam near Pella, Iowa","docAbstract":"Previous studies have shown direct evidence of under-seepage at Red Rock Dam on the Des Moines River near Pella, Iowa. Underseepage is thought to occur primarily on the northeast side of the dam in the lower bedrock of the St. Louis Limestone, which consists of discontinuous basal evaporite beds and an overlying cavity zone. Because of concerns about the integrity of the dam, the U.S. Army Corps of Engineers initiated a remedial grouting program in September 1991. To assess the effectiveness of the remedial grouting program and to evaluate methods for future assessments, a study was conducted by the U.S. Geological Survey in cooperation with the U.S. Army Corps of Engineers.
\nPotentiometric surface maps of the overburden and bedrock indicate that the direction of ground-water flow on the northeast side of the dam has changed little from pre-grout to post-grout periods. A comparison of water levels, between a pre-grout date and a post-grout date, shows that water levels decreased but that the decrease may be more attributable to changes in dam operations than to remedial grouting. Waterlevel data for the same two dates indicate that a more gradual potentiometric surface exists on the northeast side of the dam than on the southwest side of the dam, which suggests that the hydraulic connection between Lake Red Rock and downgradient bedrock wells still is greater on the northeast side of the dam than on the southwest side. Hydrographs for some wells on the northeast side of the dam indicated a departure from pre-grout trends at approximately the same time grouting was initiated. To varying degrees, hydrographs for the same wells then appear to return to a trend similar to pre-grout years, possibly as a result of new flow paths developing over time after remedial grouting. Spearman correlation coefficients computed for water levels in wells, pool, and tailwater indicate that some areas on the northeast side of the dam appear to be less under the influence of changing pool elevations after grouting than before grouting. This suggests that the hydraulic connection between the Red Rock pool and some downgradient areas has decreased.
\nAnalysis of water samples collected from selected wells on the northeast side of the dam shows significant increases in sulfate concentrations beginning about the same time remedial grouting was done upgradient from the wells, possibly indicating that flow paths were cut off to these wells, thereby reducing the amount of mixing with fresh reservoir water. Observable changes in chloride concentrations or trends as a result of remedial grouting were not apparent. Analysis results for hydrogen and oxygen stable isotope samples collected since 1995 indicate large seasonal fluctuations of isotope ratios in the tailwater (assumed representative of the reservoir). Similar but more subdued fluctuations were observed at some wells, but other wells appeared to have little seasonal change. Stable sulfur isotope results indicate the presence of distinct water types between Lake Red Rock and in ground water from downgradient bedrock wells. Sulfur isotope values from samples from a bedrock well located upgradient from the grout curtain indicate a mixture of pool and ground water, whereas samples from downgradient overburden wells have values similar to the pool. Samples from the bedrock wells downgradient from the grout curtain have sulfur isotope values similar to a value obtained from analysis of a gypsum and anhydrite core sample.
\nHydrographs, statistical analysis of waterlevel data, and water-chemistry data suggest that underseepage on the northeast side of the dam has been reduced but not completely eliminated. Some areas appear to have been affected to a greater degree and for a longer period of time than other areas. Future monitoring of water levels, water chemistry, and stable isotopes can aid in the evaluation of the long-term effectiveness of remedial grouting.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004231","collaboration":"Prepared in cooperation with the U.S. Army Corps of Engineers Rock Island District, Rock Island, Illinois","usgsCitation":"Linhart, S., and Schaap, B.D., 2001, Effects of remedial grouting on the ground-water flow system at Red Rock Dam near Pella, Iowa: U.S. Geological Survey Water-Resources Investigations Report 2000-4231, v, 35 p., https://doi.org/10.3133/wri004231.","productDescription":"v, 35 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":316675,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri004231.JPG"},{"id":2786,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://ia.water.usgs.gov/pubs/reports/WRIR_00-4231.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Iowa","otherGeospatial":"Red Rock Dam","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -92.96545028686523,\n 41.38212180399892\n ],\n [\n -92.96828269958496,\n 41.3802863707537\n ],\n [\n -92.97055721282959,\n 41.37845088570654\n ],\n [\n -92.97330379486084,\n 41.376518740220305\n ],\n [\n -92.97484874725342,\n 41.37535942537781\n ],\n [\n -92.97738075256348,\n 41.373427188056084\n ],\n [\n -92.98017024993895,\n 41.3712372497054\n ],\n [\n -92.98265933990479,\n 41.36949812849777\n ],\n [\n -92.98527717590332,\n 41.36750130237204\n ],\n [\n -92.98707962036131,\n 41.36595533037855\n ],\n [\n -92.98879623413086,\n 41.36434490382504\n ],\n [\n -92.98892498016357,\n 41.36192918926284\n ],\n [\n -92.98669338226318,\n 41.36128498356731\n ],\n [\n -92.98373222351074,\n 41.36134940442383\n ],\n [\n -92.9814577102661,\n 41.36286327619405\n ],\n [\n -92.98012733459473,\n 41.365053496418994\n ],\n [\n -92.97836780548096,\n 41.366502866327224\n ],\n [\n -92.97660827636719,\n 41.36827427459402\n ],\n [\n -92.97574996948242,\n 41.368982824396916\n ],\n [\n -92.9721450805664,\n 41.37027107699629\n ],\n [\n -92.96729564666748,\n 41.37358821002511\n ],\n [\n -92.96536445617674,\n 41.37481196396403\n ],\n [\n -92.96296119689941,\n 41.37696957930098\n ],\n [\n -92.9622745513916,\n 41.3787729043739\n ],\n [\n -92.96188831329346,\n 41.380640581203295\n ],\n [\n -92.96347618103027,\n 41.38196080315539\n ],\n [\n -92.96545028686523,\n 41.38212180399892\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db6116d2","contributors":{"authors":[{"text":"Linhart, S. Mike","contributorId":61073,"corporation":false,"usgs":true,"family":"Linhart","given":"S. Mike","affiliations":[],"preferred":false,"id":204261,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schaap, Bryan D.","contributorId":63438,"corporation":false,"usgs":true,"family":"Schaap","given":"Bryan","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":204262,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":31233,"text":"ofr0173 - 2001 - Summary of trends and status analysis for flow, nutrients, and sediments at selected nontidal sites, Chesapeake Bay basin, 1985-99","interactions":[],"lastModifiedDate":"2018-02-09T09:13:28","indexId":"ofr0173","displayToPublicDate":"2001-08-01T00:00:00","publicationYear":"2001","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":"2001-73","title":"Summary of trends and status analysis for flow, nutrients, and sediments at selected nontidal sites, Chesapeake Bay basin, 1985-99","docAbstract":"Water-quality and flow data from 31 sites in nontidal portions of the Chesapeake Bay Basin were analyzed to document annual nutrient and sediment loads and trends for the period 1985 through 1999 as part of an annual reevaluation and reporting for the Chesapeake Bay Program. Annual loads were estimated by use of the U.S. Geological Survey ESTIMATOR model. Trends were estimated using linear regression. Trends were reported for monthly mean flow, monthly load, flow-adjusted concentration, and flow-weighted concentration. Median yields and concentrations were calculated to help facilitate comparisons between basins. The drought of 1999 had pronounced effects on trend results. The trend in flow increased at 4 of the 31 sites, 8 fewer sites than in 1998. Ten less significant trends were estimated for nutrient and sediment loads compared to 1985-98. Trends in flow-weighted and flow-adjusted concentrations varied little by nutrient species and geographic location. Trends were generally downward or not significant for both the nitrogen and phosphorus species throughout the Chesapeake Bay Basin. Trends in flow-adjusted concentration indicated downward trends at most sites for nutrients and about half the sites for sediments, an indication that management actions are reducing nutrient and sediment concentrations.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr0173","usgsCitation":"Langland, M., Edwards, R.E., Sprague, L., and Yochum, S., 2001, Summary of trends and status analysis for flow, nutrients, and sediments at selected nontidal sites, Chesapeake Bay basin, 1985-99: U.S. Geological Survey Open-File Report 2001-73, 49 p., https://doi.org/10.3133/ofr0173.","productDescription":"49 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":160559,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2001/0073/coverthb.jpg"},{"id":2802,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2001/0073/ofr20010073.pdf","text":"Report","size":"1.81 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 2001-0073"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
The Red River of the North is a complex river system in the north-central plains of the United States. The river continues to impact the people and property within its basin. During the spring of 2001, major flooding occurred for the second time in four years on the Red River of the North and its many tributaries in eastern North Dakota and western Minnesota. Unlike the 1997 floods, which were the result of record-high snowpacks region-wide and a late spring blizzard, the 2001 floods were the result of above-average soil moistures in some areas of the basin, rapid melting of above-average snowpacks in the upper basin, and heavy rainfall that swept across the region on April 7, 2001.
The U.S. Geological Survey (USGS), one of the principal Federal agencies responsible for the collection and interpretation of water-resources data, works with other Federal, State, and local agencies to ensure that accurate and timely data are available for making decisions regarding the public's welfare. This report presents preliminary water-resources 2001 flood data that were obtained from selected streamflow-gaging stations located in the Red River of the North Basin.
Flooding in eastern North Dakota and western Minnesota usually is caused by spring snowmelt, and the severity of the flooding is affected by (1) substantial precipitation in the fall that produces high levels of soil moisture, (2) above-normal snowfall in the winter, (3) moist, frozen ground that prohibits infiltration of moisture, (4) a late spring thaw, (5) above-normal precipitation during spring thaw, and (6) ice jams (temporary dams of ice) on rivers and streams.
Stream stages (height of water in a stream above an arbitrarily established datum) and discharges measured by USGS personnel at streamflow-gaging stations are used to define a unique relation between stage and discharge. This relation, commonly called a rating curve, may not be well defined at extreme high discharges because these discharges are rare events of short duration and have unstable conditions that often make measurement extremely difficult. Therefore, estimates for some peak discharges need to be extrapolated from rating curves extended to known peak stages. The peak discharges are used to determine the probability, often expressed in recurrence intervals, that a given discharge will be exceeded in the future. For example, a flood that has a 1-percent chance of exceedance in any given year would, on the long-term average, be expected to occur only about once a century; therefore, the flood would be termed a \"100-year flood.\" However, the chance of such a flood occurring in any given year is 1 percent. Thus, a 100-year flood can occur in successive years at the same location. In some instances, recurrence interval estimates can be based on periods of regulated flow or made with historic adjustments when historic data are available.
Historical peak stages and peak discharges and the 2001 peak stages, peak discharges, and recurrence intervals are shown in table 1. The streamflow-gaging stations are listed in downstream order by station number, and station locations are shown in figure 1. Revisions to the 2001 peak stages and peak discharges given in this preliminary report may occur as site surveys are completed and additional field data are reviewed in the upcoming months.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr01169","collaboration":"Prepared in cooperation with the North Dakota State Water Commission","usgsCitation":"Macek-Rowland, K., 2001, 2001 floods in the Red River of the North basin in eastern North Dakota and western Minnesota: U.S. Geological Survey Open-File Report 2001-169, 8 p., https://doi.org/10.3133/ofr01169.","productDescription":"8 p.","onlineOnly":"Y","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":354174,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2001/0169/ofr20010169.pdf","text":"Report","size":"1.76 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 2001–0169"},{"id":161414,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2001/0169/report-thumb.jpg"}],"contact":"Annual loads and flow-adjusted concentration trends were estimated by use of water-quality and streamflow data collected from 1990 through 1999 at monitoring stations on two tributaries to Chesapeake Bay in Virginia—James River at Cartersville, Va., and Rappahannock River near Fredericksburg, Va. The effects of storm-sampling frequency on the accuracy and precision of load and trend estimates were determined by use of data sets containing 0, 20, 40, 60, 80, and 100 percent of all storm samples collected in these two basins of different size, relief, and land use. Data sets included a range of dissolved and particulate constituents for the 10-year period from 1990 to 1999 and the 5-year period from 1995 to 1999.
Loads of dissolved constituents were estimated with greater accuracy and precision with fewer storm samples than loads of particulate constituents in both basins and for both time periods. All constituent loads were estimated with greater precision with fewer storm samples in the James River than in the Rappahannock River for both periods. The high relief and smaller drainage area of the Rappahannock River Basin caused quicker and more variable stream response than in the James River Basin, which led to less precise load estimates of all constituents, regardless of how many storm samples were included. For the James River, the magnitudes of the load estimates in the 5-year period were close to the estimates from the same years for the 10-year period for the dissolved constituents, but were smaller for the particulate constituents. Load estimates were more variable for the Rappahannock River than for the James River during the shorter period. In both basins, all estimates in the 5-year period had higher prediction errors than those in the 10-year period. Overall, loads of dissolved constituents were estimated with greater accuracy and precision with fewer storm samples than loads of particulate constituents; loads of all constituents were estimated with greater accuracy and precision over the longer time period; and load estimates of all constituents were more precise and required fewer storm samples in the larger and less flashy James River Basin than in the Rappahannock River Basin.
As with load estimates, estimates of flow-adjusted concentration trends were sensitive to the length of the monitoring period and the size of the basin; however, trend estimates generally were less sensitive than load estimates to the number of storm samples in the data set. Trends in flow-adjusted concentrations were estimated reasonably well with fewer storm samples for both dissolved and particulate constituents in the James River for the 10-year period, with the exception of total suspended solids. Data sets containing more storm samples were needed to obtain reasonable trend estimates for the 5-year period in this river. For the 10-year period in the Rappahannock River, more storm samples were necessary than in the James River to obtain reasonable estimates of trends for all constituents. No significant trends were observed for the 5-year period in this river, so the effect of storm-sampling frequency could not be determined. Because of the small number of significant trends throughout these data sets, it was not possible to determine whether fewer storm samples were required for estimating trends of dissolved constituents than particulate constituents. The results indicate that more storm samples were necessary for accurate estimation of trends during the shorter time period and in the smaller and flashier Rappahannock River Basin.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri014136","collaboration":"Prepared in cooperation with the Virginia Department of Environmental Quality","usgsCitation":"Sprague, L., 2001, Effects of storm-sampling frequency on estimation of water-quality loads and trends in two tributaries to Chesapeake Bay in Virginia: U.S. Geological Survey Water-Resources Investigations Report 2001-4136, 38 p., https://doi.org/10.3133/wri014136.","productDescription":"38 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":614,"text":"Virginia Water Science Center","active":true,"usgs":true}],"links":[{"id":2907,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4136/wri20014136.pdf","text":"Report","size":"974 KB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2001-4136"},{"id":161229,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2001/4136/coverthb.jpg"}],"contact":"Director, Virginia Water Science Center
U.S. Geological Survey
1730 East Parham Road
Richmond, VA 23228