Volcanic rocks, mostly basalts and some andesites, are interbedded with middle Miocene strata and are overlain by younger rocks throughout the greater part of the Los Angeles Basin, California. Roughly correlative flows, previously dated radiometrically (or paleontologically) at about 16.4 to 10.7 Ma, crop out in five separate regions around the basin perimeter. Los Angeles Basin volcanic rocks have special meaning because they offer clues to tectonomagmatic events associated with onset of clockwise transrotation of the western Transverse Ranges region and to the timing and locus of the initial basin opening.
\nWhole-rock 40Ar/39Ar dating of near-tholeiitic olivine basalts of the Topanga Formation (Hoots, 1931) from three sites in the easternmost Santa Monica Mountains, combined with 87Sr/86Sr dating of fossil carbonates from interstratified marine beds at nine sites, establish a new age of 17.4 Ma for these oldest known Topanga-age volcanics of the Los Angeles Basin. We also record three new 40Ar/39Ar ages (15.3 Ma) from andesitic flows of the lower Glendora Volcanics at the northeast edge of the basin, 70 km east of the Santa Monica Mountains. A whole-rock determination of 17.2±0.5 Ma for nearby altered olivine basalt in the unfossiliferous Glendora volcanic sequence is questionable because of a complex 40Ar/39Ar age spectrum suggestive of 39Ar recoil, but it may indicate an older volcanic unit in this eastern area.
\nWe hypothesize that the 17.4-Ma volcanics in the eastern Santa Monica Mountains are an early expression of deep crustal magmatism accompanying the earliest extensional tectonism associated with rifting. The extremely thick younger volcanic pile in the western and central parts of the range may suggest that this early igneous activity in the eastern area was premonitory. Paleomagnetic declination data are needed to determine the pre-transrotational orientation of the eastern Santa Monica Mountains volcanic sequence. The new age determinations do not yield unequivocal support for either of two proposed explanations of possible age trends of Miocene volcanic rocks in southern California but underscore the need for further work.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/pp1669","usgsCitation":"McCulloh, T.H., Fleck, R.J., Denison, R.E., Beyer, L.A., and Stanley, R.G., 2002, Age and tectonic significance of volcanic rocks in the northern Los Angeles Basin, California: U.S. Geological Survey Professional Paper 1669, iii, 24 p., https://doi.org/10.3133/pp1669.","productDescription":"iii, 24 p.","numberOfPages":"27","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":81988,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1669/pdf/pp1669.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124313,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1669/report-thumb.jpg"},{"id":3770,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1669/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"California","otherGeospatial":"Los Angeles Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -118.5,33.5 ], [ -118.5,34.25 ], [ -117.75,34.25 ], [ -117.75,33.5 ], [ -118.5,33.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae3e4b07f02db6896e8","contributors":{"authors":[{"text":"McCulloh, Thane H.","contributorId":100450,"corporation":false,"usgs":true,"family":"McCulloh","given":"Thane","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":230245,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fleck, Robert J. 0000-0002-3149-8249 fleck@usgs.gov","orcid":"https://orcid.org/0000-0002-3149-8249","contributorId":1048,"corporation":false,"usgs":true,"family":"Fleck","given":"Robert","email":"fleck@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":230241,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Denison, Rodger E.","contributorId":42994,"corporation":false,"usgs":true,"family":"Denison","given":"Rodger","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":230244,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Beyer, Larry A. lbeyer@usgs.gov","contributorId":2819,"corporation":false,"usgs":true,"family":"Beyer","given":"Larry","email":"lbeyer@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":230243,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Stanley, Richard G. 0000-0001-6192-8783 rstanley@usgs.gov","orcid":"https://orcid.org/0000-0001-6192-8783","contributorId":1832,"corporation":false,"usgs":true,"family":"Stanley","given":"Richard","email":"rstanley@usgs.gov","middleInitial":"G.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":230242,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":44567,"text":"wri024238 - 2002 - Flow-frequency characteristics of Vermont streams","interactions":[],"lastModifiedDate":"2012-02-02T00:04:53","indexId":"wri024238","displayToPublicDate":"2003-03-01T00:00:00","publicationYear":"2002","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4238","title":"Flow-frequency characteristics of Vermont streams","docAbstract":"The safe and economical design of infrastructure in and near waterways and the effective management of flood-hazard areas require information on streamflow that may not be readily available. This report provides estimates of flow-frequency characteristics for gaged streams in Vermont and describes methods for estimating flow-frequency characteristics for ungaged streams. The flow-frequency characteristics investigated are the magnitude of peak discharges at recurrence intervals of 2, 5, 10, 25, 50, 100, and 500 years, and the magnitude of daily-mean discharges exceeded 25, 50, and 75 percent of the time.\r\n\r\nPeak-flow frequency characteristics for gaged streams were computed following the guidelines in Bulletin 17B of the U.S. Interagency Advisory Committee on Water Data. To determine the peak-flow exceedance probabilities at stream-gaging stations in Vermont, a new generalized skew coefficient map for the State was developed. This new map has greater resolution and more current data than the existing National map. The standard error of the new map is 0.269.\r\n\r\nTwo methods of extending streamflow record were applied to improve estimates of peak-flow frequency for streams with short flow records (10 to 15 years) in small drainage areas (sites less than 15 square miles). In the first method, a two-station comparison, data from a long-record site was used to adjust the frequency characteristics at the short-record site. This method was applied to 31 crest-stage gages--stations at which only instantaneous peak discharges are determined--in Vermont. The second method used rainfall-runoff modeling. Precipitation and evapotranspiration data from 1948 to 1999 for numerous climate data-collection sites were used as input to a model to simulate flows at 10 stream-gaging stations in Vermont.\r\n\r\nAlso, methods are described to estimate flow-frequency characteristics for ungaged and unregulated rural streams in Vermont. The peak-flow estimating methods were developed by generalized-least-squares regression procedures with data from 138 U.S. Geological Survey stream-gaging stations in Vermont and in adjacent areas of New York, New Hampshire, Massachusetts, and Quebec. The flow-duration (daily flow exceeded a given percentage of the time) estimating methods were developed by ordinary-least-squares regression procedures with data from 81 stream-gaging stations in Vermont and adjacent states.","language":"ENGLISH","doi":"10.3133/wri024238","usgsCitation":"Olson, S.A., 2002, Flow-frequency characteristics of Vermont streams: U.S. Geological Survey Water-Resources Investigations Report 2002-4238, iv, 47 p. : ill., maps ; 28 cm., https://doi.org/10.3133/wri024238.","productDescription":"iv, 47 p. : ill., maps ; 28 cm.","costCenters":[],"links":[{"id":135008,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":3783,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri024238/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b25e4b07f02db6aee4b","contributors":{"authors":[{"text":"Olson, Scott A. 0000-0002-1064-2125 solson@usgs.gov","orcid":"https://orcid.org/0000-0002-1064-2125","contributorId":2059,"corporation":false,"usgs":true,"family":"Olson","given":"Scott","email":"solson@usgs.gov","middleInitial":"A.","affiliations":[{"id":405,"text":"NH/VT office of New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":230009,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47756,"text":"wri024234 - 2002 - Simulation of ground-water flow and evaluation of water-management alternatives in the upper Charles River basin, eastern Massachusetts","interactions":[],"lastModifiedDate":"2025-09-11T13:37:32.812392","indexId":"wri024234","displayToPublicDate":"2003-03-01T00:00:00","publicationYear":"2002","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4234","title":"Simulation of ground-water flow and evaluation of water-management alternatives in the upper Charles River basin, eastern Massachusetts","docAbstract":"Ground water is the primary source of drinking water for towns in the upper Charles River Basin, an area of 105 square miles in eastern Massachusetts that is undergoing rapid growth. The stratified-glacial aquifers in the basin are high yield, but also are thin, discontinuous, and in close hydraulic connection with streams, ponds, and wetlands. Water withdrawals averaged 10.1 million gallons per day in 1989?98 and are likely to increase in response to rapid growth. These withdrawals deplete streamflow and lower pond levels. A study was conducted to develop tools for evaluating water-management alternatives at the regional scale in the basin. Geologic and hydrologic data were compiled and collected to characterize the ground- and surface-water systems. Numerical flow modeling techniques were applied to evaluate the effects of increased withdrawals and altered recharge on ground-water levels, pond levels, and stream base flow. Simulation-optimization methods also were applied to test their efficacy for management of multiple water-supply and water-resource needs. \r\n\r\nSteady-state and transient ground-water-flow models were developed using the numerical modeling code MODFLOW-2000. The models were calibrated to 1989?98 average annual conditions of water withdrawals, water levels, and stream base flow. Model recharge rates were varied spatially, by land use, surficial geology, and septic-tank return flow. Recharge was changed during model calibration by means of parameter-estimation techniques to better match the estimated average annual base flow; area-weighted rates averaged 22.5 inches per year for the basin. Water withdrawals accounted for about 7 percent of total simulated flows through the stream-aquifer system and were about equal in magnitude to model-calculated rates of ground-water evapotranspiration from wetlands and ponds in aquifer areas. Water withdrawals as percentages of total flow varied spatially and temporally within an average year; maximum values were 12 to 13 percent of total annual flow in some subbasins and of total monthly flow throughout the basin in summer and early fall. \r\n\r\nWater-management alternatives were evaluated by simulating hypothetical scenarios of increased withdrawals and altered recharge for average 1989?98 conditions with the flow models. Increased withdrawals to maximum State-permitted levels would result in withdrawals of about 15 million gallons per day, or about 50 percent more than current withdrawals. Model-calculated effects of these increased withdrawals included reductions in stream base flow that were greatest (as a percentage of total flow) in late summer and early fall. These reductions ranged from less than 5 percent to more than 60 percent of model-calculated 1989?98 base flow along reaches of the Charles River and major tributaries during low-flow periods. Reductions in base flow generally were comparable to upstream increases in withdrawals, but were slightly less than upstream withdrawals in areas where septic-system return flow was simulated. Increased withdrawals also increased the proportion of wastewater in the Charles River downstream of treatment facilities. The wastewater component increased downstream from a treatment facility in Milford from 80 percent of September base flow under 1989?98 conditions to 90 percent of base flow, and from 18 to 27 percent of September base flow downstream of a treatment facility in Medway. In another set of hypothetical scenarios, additional recharge equal to the transfer of water out of a typical subbasin by sewers was found to increase model-calculated base flows by about 12 percent of model-calculated base flows. Addition of recharge equal to that available from artificial recharge of residential rooftop runoff had smaller effects, augmenting simulated September base flow by about 3 percent. \r\n\r\nSimulation-optimization methods were applied to an area near Populatic Pond and the confluence of the Mill and Charles Rivers in Franklin,","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri024234","usgsCitation":"DeSimone, L., Walter, D.A., Eggleston, J.R., and Nimiroski, M.T., 2002, Simulation of ground-water flow and evaluation of water-management alternatives in the upper Charles River basin, eastern Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 2002-4234, vii, 94 p., https://doi.org/10.3133/wri024234.","productDescription":"vii, 94 p.","costCenters":[],"links":[{"id":170495,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":4083,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri024234/index.html","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Massachusetts","otherGeospatial":"upper Charles River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -71.667,\n 42.25\n ],\n [\n -71.667,\n 41.9\n ],\n [\n -71.1958,\n 41.9\n ],\n [\n -71.1958,\n 42.25\n ],\n [\n -71.667,\n 42.25\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f8e4b07f02db5f2e4d","contributors":{"authors":[{"text":"DeSimone, Leslie A. 0000-0003-0774-9607 ldesimon@usgs.gov","orcid":"https://orcid.org/0000-0003-0774-9607","contributorId":176711,"corporation":false,"usgs":true,"family":"DeSimone","given":"Leslie A.","email":"ldesimon@usgs.gov","affiliations":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":false,"id":236165,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Walter, Donald A. 0000-0003-0879-4477 dawalter@usgs.gov","orcid":"https://orcid.org/0000-0003-0879-4477","contributorId":1101,"corporation":false,"usgs":true,"family":"Walter","given":"Donald","email":"dawalter@usgs.gov","middleInitial":"A.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236164,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Eggleston, John R. 0000-0001-6633-3041 jegglest@usgs.gov","orcid":"https://orcid.org/0000-0001-6633-3041","contributorId":3068,"corporation":false,"usgs":true,"family":"Eggleston","given":"John","email":"jegglest@usgs.gov","middleInitial":"R.","affiliations":[{"id":614,"text":"Virginia Water Science Center","active":true,"usgs":true}],"preferred":true,"id":236166,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Nimiroski, Mark T.","contributorId":65898,"corporation":false,"usgs":true,"family":"Nimiroski","given":"Mark","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":236167,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":50567,"text":"ofr02455 - 2002 - User guide for the PULSE program","interactions":[],"lastModifiedDate":"2012-02-02T00:11:17","indexId":"ofr02455","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2002","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":"2002-455","title":"User guide for the PULSE program","docAbstract":"This manual describes the use of the PULSE computer program for analysis of streamflow records. The specific instructions included here and the computer files that accompany this manual require streamflow data in a format that can be obtained from U.S. Geological Survey (USGS) sites on the World Wide Web. The program is compiled to run on a personal computer that uses a Microsoft Windows-based operating system. This manual provides instructions for use of Microsoft Excel for plotting hydrographs, though users may choose to use other software for plotting. The program calculates a hydrograph of ground-water discharge to a stream on the basis of user-specified recharge to the water table. Two different formulations allow recharge to be treated as instantaneous quantities or as gradual rates. The process of ground-water evapotranspiration can be approximated as a negative gradual recharge. The PULSE program is intended for analyzing a ground-water-flow system that is characterized by diffuse areal recharge to the water table and ground-water discharge to a stream. Program use can be appropriate if all or most ground water in the basin discharges to the stream and if a streamflow-gaging station at the downstream end of the basin measures all or most outflow. Ground-water pumpage and the regulation and diversion of streamflow should be negligible. More information about the application of the method is included in Rutledge, 1997, pages 2-3. The program can be used in conjunction with ground-water-level data. If a well is open to the surficial aquifer, observed water-level rises in the well can be used to evaluate the timing of recharge. Such evaluation is most effective if there are numerous water-level observation wells in the basin. Water levels in observation wells can also be used to evaluate the rate of ground-water discharge estimated by the PULSE program. The results of such an evaluation may be problematic, however, because the relation between ground-water level and ground-water discharge may not be unique. Departures from the linear model of recession occur because of areal variation in transmissivity and because of the longitudinal component of ground-water flow (parallel to the stream). If the PULSE program is used to estimate ground-water recharge, the recession index should not be obtained from periods of extreme low flow, and the calibration process should include plotting flow on the linear scale in addition to plotting flow on the log scale.","language":"ENGLISH","doi":"10.3133/ofr02455","usgsCitation":"Rutledge, A.T., 2002, User guide for the PULSE program: U.S. Geological Survey Open-File Report 2002-455, p. 34, illus., 16 refs, https://doi.org/10.3133/ofr02455.","productDescription":"p. 34, illus., 16 refs","costCenters":[],"links":[{"id":175490,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":4377,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2002/ofr02-455/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e486ce4b07f02db50b72e","contributors":{"authors":[{"text":"Rutledge, A. T.","contributorId":38532,"corporation":false,"usgs":true,"family":"Rutledge","given":"A.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":241850,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":44982,"text":"wri024102 - 2002 - A three-dimensional numerical model of predevelopment conditions in the Death Valley regional ground-water flow system, Nevada and California","interactions":[],"lastModifiedDate":"2012-02-02T00:10:12","indexId":"wri024102","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2002","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4102","title":"A three-dimensional numerical model of predevelopment conditions in the Death Valley regional ground-water flow system, Nevada and California","docAbstract":"In the early 1990's, two numerical models of the Death Valley regional ground-water flow system were developed by the U.S. Department of Energy. In general, the two models were based on the same basic hydrogeologic data set. In 1998, the U.S. Department of Energy requested that the U.S. Geological Survey develop and maintain a ground-water flow model of the Death Valley region in support of U.S. Department of Energy programs at the Nevada Test Site. The purpose of developing this 'second-generation' regional model was to enhance the knowledge an understanding of the ground-water flow system as new information and tools are developed. The U.S. Geological Survey also was encouraged by the U.S. Department of Energy to cooperate to the fullest extent with other Federal, State, and local entities in the region to take advantage of the benefits of their knowledge and expertise.\r\n\r\n \r\n\r\nThe short-term objective of the Death Valley regional ground-water flow system project was to develop a steady-state representation of the predevelopment conditions of the ground-water flow system utilizing the two geologic interpretations used to develop the previous numerical models. The long-term objective of this project was to construct and calibrate a transient model that simulates the ground-water conditions of the study area over the historical record that utilizes a newly interpreted hydrogeologic conceptual model. This report describes the result of the predevelopment steady-state model construction and calibration.\r\n\r\n \r\n\r\nThe Death Valley regional ground-water flow system is situated within the southern Great Basin, a subprovince of the Basin and Range physiographic province, bounded by latitudes 35 degrees north and 38 degrees 15 minutes north and by longitudes 115 and 118 degrees west. Hydrology in the region is a result of both the arid climatic conditions and the complex geology. Ground-water flow generally can be described as dominated by interbasinal flow and may be conceptualized as having two main components: a series of relatively shallow and localized flow paths that are superimposed on deeper regional flow paths. A significant component of the regional ground-water flow is through a thick Paleozoic carbonate rock sequence. Throughout the flow system, ground water flows through zones of high transmissivity that have resulted from regional faulting and fracturing.\r\n\r\n \r\n\r\nThe conceptual model of the Death Valley regional ground-water flow system used for this study is adapted from the two previous ground-water modeling studies. The three-dimensional digital hydrogeologic framework model developed for the region also contains elements of both of the hydrogeologic framework models used in the previous investigations. As dictated by project scope, very little reinterpretation and refinement were made where these two framework models disagree; therefore, limitations in the hydrogeologic representation of the flow system exist. Despite limitations, the framework model provides the best representation to date of the hydrogeologic units and structures that control regional ground-water flow and serves as an important information source used to construct and calibrate the predevelopment, steady-state flow model.\r\n\r\n \r\n\r\nIn addition to the hydrogeologic framework, a complex array of mechanisms accounts for flow into, through, and out of the regional ground-water flow system. Natural discharges from the regional ground-water flow system occur by evapotranspiration, springs, and subsurface outflow. In this study, evapotranspiration rates were adapted from a related investigation that developed maps of evapotranspiration areas and computed rates from micrometeorological data collected within the local area over a multiyear period. In some cases, historical spring flow records were used to derive ground-water discharge rates for isolated regional springs.\r\n\r\n \r\n\r\nFor this investigation, a process-based, numerical model was developed to estimat","language":"ENGLISH","doi":"10.3133/wri024102","usgsCitation":"D’Agnese, F.A., O’Brien, G.M., Faunt, C., Belcher, W., and San Juan, C., 2002, A three-dimensional numerical model of predevelopment conditions in the Death Valley regional ground-water flow system, Nevada and California: U.S. Geological Survey Water-Resources Investigations Report 2002-4102, viii, 114 p. : ill. (some col.), col. maps ; 28 cm., https://doi.org/10.3133/wri024102.","productDescription":"viii, 114 p. : ill. (some col.), col. maps ; 28 cm.","costCenters":[],"links":[{"id":161720,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":3857,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri024102/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b16e4b07f02db6a5650","contributors":{"authors":[{"text":"D’Agnese, Frank A.","contributorId":47810,"corporation":false,"usgs":true,"family":"D’Agnese","given":"Frank","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":230832,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O’Brien, G. M.","contributorId":31407,"corporation":false,"usgs":true,"family":"O’Brien","given":"G.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":230831,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Faunt, C.C. 0000-0001-5659-7529","orcid":"https://orcid.org/0000-0001-5659-7529","contributorId":103314,"corporation":false,"usgs":true,"family":"Faunt","given":"C.C.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":230834,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Belcher, W.R.","contributorId":30667,"corporation":false,"usgs":true,"family":"Belcher","given":"W.R.","email":"","affiliations":[],"preferred":false,"id":230830,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"San Juan, C. 0000-0002-9151-1919","orcid":"https://orcid.org/0000-0002-9151-1919","contributorId":83974,"corporation":false,"usgs":true,"family":"San Juan","given":"C.","affiliations":[],"preferred":false,"id":230833,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":44638,"text":"wri014249 - 2002 - Comparisons of water quality during various streamflow conditions in five streams in northern New Jersey, 1982-97","interactions":[],"lastModifiedDate":"2016-02-29T11:10:35","indexId":"wri014249","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2002","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":"2001-4249","title":"Comparisons of water quality during various streamflow conditions in five streams in northern New Jersey, 1982-97","docAbstract":"Relations between water-quality and flow characteristics and the relative importance of constant (point sources and ground-water discharge) and intermittent (nonpoint storm runoff) sources were determined for eight water-quality stations located on the Flat Brook and the Delaware, Musconetcong, Whippany, and Saddle Rivers. Water-quality and streamflow data were categorized on the basis of streamflow at the time of sample collection. Differences in concentrations and yields of selected water-quality constituents, including nutrients and bacteria, (1) among the stations during eight streamflow conditions and (2) at each station (a) between base flow and stormflow; (b) among before, during, and after a storm; and (c) among low, medium, and high flows were determined and related to the predominant type(s) of land development in the areas contributing drainage. At the station on the Delaware River, yields of fecal-coliform bacteria were affected more by contributions from storm runoff than by contributions from point sources and ground-water discharges; yields during a storm [7.0 x 108 (MPN/d)mi2 (most probable number per day per square mile)] were greater than yields during base flow (3.7 x 108 (MPN/d)mi2). Yields of nitrate plus nitrite, alkalinity, and chloride were affected more by contributions from point sources and ground-water discharges than by contributions from storm runoff; yields of these constituents were not significantly different during base flows and stormflows. At the Flat Brook and Whippany River stations, yields of most water-quality constituents were affected more by contributions from storm runoff than by contributions from point sources and ground-water discharge. For example, yields of nitrate plus nitrite were greater during stormflow (1.20 (lb/d)/mi2 (pounds per day per square mile) and 15.88 (lb/d)/mi2, respectively) than during base flow (0.26 (lb/d)/mi2 and 8.20 (lb/d)/mi2, respectively). At the Musconetcong River station, yields of total nitrogen, alkalinity, and chloride were affected more by contributions from storm runoff than by contributions from point sources and ground-water discharge. At three of the four water-quality stations on the Musconetcong River, yields of total phosphorus and bacteria were affected less by contributions from storm runoff than by contributions from point sources and ground-water discharge. At the Saddle River station, yields of alkalinity and chloride were affected more by contributions from storm runoff than by contributions from point sources and ground-water discharge; for example, yields of chloride during stormflows (707 (lb/d)/mi2) were greater than during base flows (401 (lb/d)/mi2). Yields of total phosphorus were affected less by contributions from storm runoff than by contributions from point sources and ground-water discharge; yields during base flows (4.00 (lb/d)/mi2) and stormflows (4.67 (lb/d)/mi2) were similar. Concentrations and yields of total phosphorus and nitrogen, and nitrate plus nitrite were strongly related to the amount of development in each drainage basin. At stations on the Saddle and Whippany Rivers, which drain areas with substantial development, concentrations and yields for all streamflow categories were higher than at stations on the Flat Brook and Delaware River, which drain areas with little development. Results of the Tukey test indicate that there are significant differences in total phosphorus concentrations at Saddle River and Flat Brook during base flows (0.77 mg/L (milligrams per liter) and 0.02 mg/L, respectively) and stormflows (0.42 mg/L and 0.02 mg/L, respectively).
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"West Trenton, NJ","doi":"10.3133/wri014249","usgsCitation":"Hunchak-Kariouk, K., 2002, Comparisons of water quality during various streamflow conditions in five streams in northern New Jersey, 1982-97: U.S. Geological Survey Water-Resources Investigations Report 2001-4249, v, 40 p., https://doi.org/10.3133/wri014249.","productDescription":"v, 40 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":168544,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri014249.PNG"},{"id":3728,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2001/4249/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Jersey","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.0640869140625,\n 40.42395127765169\n ],\n [\n -74.2510986328125,\n 40.486648520560806\n ],\n [\n -73.89678955078125,\n 41.00270266805319\n ],\n [\n -74.696044921875,\n 41.35619553438905\n ],\n [\n -75.13824462890625,\n 40.9840449469281\n ],\n [\n -75.05035400390625,\n 40.865756786006806\n ],\n [\n -75.1959228515625,\n 40.7701418259051\n ],\n [\n -75.201416015625,\n 40.57224011776902\n ],\n [\n -75.15472412109375,\n 40.56806745430726\n ],\n [\n -75.07232666015625,\n 40.54511315470123\n ],\n [\n -75.07232666015625,\n 40.45948689837198\n ],\n [\n -75.0640869140625,\n 40.42395127765169\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ee4b07f02db6aa5e7","contributors":{"authors":[{"text":"Hunchak-Kariouk, Kathryn","contributorId":41448,"corporation":false,"usgs":true,"family":"Hunchak-Kariouk","given":"Kathryn","email":"","affiliations":[],"preferred":false,"id":230165,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":44606,"text":"wri20024141 - 2002 - Results of Hydraulic Tests in Miocene Tuffaceous Rocks at the C-Hole Complex, 1995 to 1997, Yucca Mountain, Nye County, Nevada","interactions":[],"lastModifiedDate":"2012-02-10T00:10:10","indexId":"wri20024141","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2002","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4141","title":"Results of Hydraulic Tests in Miocene Tuffaceous Rocks at the C-Hole Complex, 1995 to 1997, Yucca Mountain, Nye County, Nevada","docAbstract":"Four hydraulic tests were conducted by the U.S. Geological Survey at the C-hole complex at Yucca Mountain, Nevada, between May 1995 and November 1997. These tests were conducted as part of ongoing investigations to determine the hydrologic and geologic suitability of Yucca Mountain as a potential site for permanent underground storage of high-level nuclear waste. \r\n\r\nThe C-hole complex consists of three 900-meter-deep boreholes that are 30.4 to 76.6 meters apart. The C-holes are completed in fractured, variably welded tuffaceous rocks of Miocene age. Six hydrogeologic intervals occur within the saturated zone in these boreholes - the Calico Hills, Prow Pass, Upper Bullfrog, Lower Bullfrog, Upper Tram, and Lower Tram intervals. The Lower Bullfrog and Upper Tram intervals contributed about 90 percent of the flow during hydraulic tests. \r\n\r\nThe four hydraulic tests conducted from 1995 to 1997 lasted 4 to 553 days. Discharge from the pumping well, UE-25 c #3, ranged from 8.49 to 22.5 liters per second in different tests. Two to seven observation wells, 30 to 3,526 meters from the pumping well, were used in different tests. Observation wells included UE-25 c #1, UE-25 c #2, UE-25 ONC-1, USW H-4, UE-25 WT #14, and UE-25 WT #3 in the tuffaceous rocks and UE-25 p #1 in Paleozoic carbonate rocks. \r\n\r\nIn all hydraulic tests, drawdown in the pumping well was rapid and large (2.9-11 meters). Attributable mostly to frictional head loss and borehole-skin effects, this drawdown could not be used to analyze hydraulic properties. Drawdown and recovery in intervals of UE-25 c #1 and UE-25 c #2 and in other observation wells typically was less than 51 centimeters. These data were analyzed. \r\n\r\nHydrogeologic intervals in the C-holes have layered heterogeneity related to faults and fracture zones. Transmissivity, hydraulic conductivity, and storativity generally increase downhole. Transmissivity ranges from 4 to 1,600 meters squared per day; hydraulic conductivity ranges from 0.1 to 50 meters per day; and storativity ranges from 0.00002 to 0.002. \r\n\r\nTransmissivity in the Miocene tuffaceous rocks decreases from 2,600 to 700 meters squared per day northwesterly across the 21-square-kilometer area affected by hydraulic tests at the C-hole complex. The average transmissivity of the tuffaceous rocks in this area, as determined from plots of drawdown in most or all observation wells as functions of time or distance from the pumping well, is 2,100 to 2,600 meters squared per day. Average storativity determined from these plot ranges is 0.0005 to 0.002. Hydraulic conductivity ranges from less than 2 to more than 10 meters per day; it is largest where prominent northerly trending faults are closely spaced or intersected by northwesterly trending faults. \r\n\r\nDuring hydraulic tests, the Miocene tuffaceous rocks functioned as a single aquifer. Drawdown occurred in all monitored intervals of the C-holes and other observation wells, regardless of the hydrogeologic interval being pumped. This hydraulic connection across geologic and lithostratigraphic contacts is believed to result from interconnected faults, fractures, and intervals with large matrix permeability. Samples of UE-25 c #3 water, analyzed from 1995 to 1997, seem to indicate that changes in the quality of the water pumped from that well are probably due solely to lateral variations in water quality within the tuffaceous rocks.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/wri20024141","collaboration":"Prepared in cooperation with the U.S. Department of Energy, Under Interagency Agreement DE?AI08?92NV10874","usgsCitation":"Geldon, A.L., Umari, A., Fahy, M., Earle, J.D., Gemmell, J.M., and Darnell, J., 2002, Results of Hydraulic Tests in Miocene Tuffaceous Rocks at the C-Hole Complex, 1995 to 1997, Yucca Mountain, Nye County, Nevada: U.S. Geological Survey Water-Resources Investigations Report 2002-4141, v, 58 p., https://doi.org/10.3133/wri20024141.","productDescription":"v, 58 p.","costCenters":[{"id":687,"text":"Yucca Mountain Project Branch","active":false,"usgs":true}],"links":[{"id":125699,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_2002_4141.jpg"},{"id":13246,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/2002/wri02-4141/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.58333333333333,36.666666666666664 ], [ -116.58333333333333,36.916666666666664 ], [ -116.33333333333333,36.916666666666664 ], [ -116.33333333333333,36.666666666666664 ], [ -116.58333333333333,36.666666666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2ce4b07f02db613d01","contributors":{"authors":[{"text":"Geldon, Arthur L.","contributorId":16395,"corporation":false,"usgs":true,"family":"Geldon","given":"Arthur","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":230083,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Umari, Amjad M.A.","contributorId":100463,"corporation":false,"usgs":true,"family":"Umari","given":"Amjad M.A.","affiliations":[],"preferred":false,"id":230086,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Fahy, Michael F.","contributorId":85630,"corporation":false,"usgs":true,"family":"Fahy","given":"Michael F.","affiliations":[],"preferred":false,"id":230085,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Earle, John D.","contributorId":34537,"corporation":false,"usgs":true,"family":"Earle","given":"John","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":230084,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Gemmell, James M.","contributorId":108176,"corporation":false,"usgs":true,"family":"Gemmell","given":"James","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":230088,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Darnell, Jon","contributorId":103323,"corporation":false,"usgs":true,"family":"Darnell","given":"Jon","affiliations":[],"preferred":false,"id":230087,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":47503,"text":"ofr02485 - 2002 - Ground-water, surface-water and water-chemistry data, Black Mesa area, northeastern Arizona: 2001-02","interactions":[],"lastModifiedDate":"2022-12-05T21:44:47.832479","indexId":"ofr02485","displayToPublicDate":"2003-02-01T00:00:00","publicationYear":"2002","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":"2002-485","title":"Ground-water, surface-water and water-chemistry data, Black Mesa area, northeastern Arizona: 2001-02","docAbstract":"The N aquifer is the major source of water in the 5,400-square-mile area of Black Mesa in northeastern Arizona. Availability of water is an important issue in this area because of continued industrial and municipal use, a growing population, and precipitation of about 6 to 14 inches per year.
\nThe monitoring program in the Black Mesa area has been operating since 1971 and is designed to determine the long-term effects of ground-water withdrawals from the N aquifer for industrial and municipal uses. The monitoring program includes measurements of (1) ground-water pumping, (2) ground-water levels, (3) spring discharge, (4) surface-water discharge, and (5) ground-water chemistry.
\nIn 2001, total ground-water withdrawals were 7,680 acre-feet, industrial use was 4,530 acre-feet, and municipal use was 3,150 acre-feet. From 2000 to 2001, total withdrawals decreased by 1 percent, industrial use increased by 1 percent, and municipal use decreased by 3 percent.
\nFrom 2001 to 2002, water levels declined in 5 of 14 wells in the unconfined part of the aquifer, and the median change was +0.2 foot. Water levels declined in 12 of 17 wells in the confined part of the aquifer, and the median change was -1.4 feet.
\nFrom the prestress period (prior to 1965) to 2002, the median water-level change for 32 wells was -15.8 feet. Median water-level changes were -1.3 feet for 15 wells in the unconfined part of the aquifer and -31.7 feet for 17 wells in the confined part.
\nDischarges were measured once in 2001 and once in 2002 at four springs. Discharges decreased by 26 percent and 66 percent at two springs, increased by 100 percent at one spring, and did not change at one spring. For the past 10 years, discharges from the four springs have fluctuated; however, an increasing or decreasing trend is not apparent.
\nContinuous records of surface-water discharge have been collected from 1976 to 2001 at Moenkopi Wash, 1996 to 2001 at Laguna Creek, 1993 to 2001 at Dinnebito Wash, and 1994 to 2001 at Polacca Wash. Median flows for November, December, January, and February of each water year were used as an index of ground-water discharge to those streams. Since 1995, the median winter flows have decreased for Moenkopi Wash, Dinnebito Wash, and Polacca Wash. Since 1997, there is no consistent trend in the median winter flow for Laguna Creek.
\nIn 2002, water samples were collected from 12 wells and 4 springs and analyzed for selected chemical constituents. Dissolved-solids concentrations ranged from 96 to 636 milligrams per liter. Water samples from 8 of the wells and from 3 of the springs had less than 300 milligrams per liter of dissolved solids. There are no appreciable time trends in the chemistry of water samples from 9 wells and 4 springs; the 9 wells had more than 7 years of data, and the 4 springs had more than 9 years of data.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Tucson, AZ","doi":"10.3133/ofr02485","collaboration":"Prepared in cooperation with the Arizona Department of Water Resources and Bureau of Indian Affairs","usgsCitation":"Thomas, B.E., 2002, Ground-water, surface-water and water-chemistry data, Black Mesa area, northeastern Arizona: 2001-02: U.S. Geological Survey Open-File Report 2002-485, iv, 43 p., https://doi.org/10.3133/ofr02485.","productDescription":"iv, 43 p.","numberOfPages":"50","costCenters":[],"links":[{"id":287827,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287826,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2002/0485/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":410071,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_54475.htm","linkFileType":{"id":5,"text":"html"}}],"scale":"100000","projection":"Lambert Conformal Conic projection","country":"United States","state":"Arizona","otherGeospatial":"Black Mesa","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -111.4,\n 36.875\n ],\n [\n -111.4,\n 35.5958\n ],\n [\n -109.5917,\n 35.5958\n ],\n [\n -109.5917,\n 36.875\n ],\n [\n -111.4,\n 36.875\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db6485e2","contributors":{"authors":[{"text":"Thomas, Blakemore E.","contributorId":93871,"corporation":false,"usgs":true,"family":"Thomas","given":"Blakemore","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":235575,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":50503,"text":"ofr02286 - 2002 - Daily values flow comparison and estimates using program HYCOMP, version 1.0","interactions":[],"lastModifiedDate":"2012-02-02T00:11:19","indexId":"ofr02286","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2002","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":"2002-286","title":"Daily values flow comparison and estimates using program HYCOMP, version 1.0","docAbstract":"A method used by the U.S. Geological Survey for quality control in computing daily value flow records is to compare hydrographs of computed flows at a station under review to hydrographs of computed flows at a selected index station. The hydrographs are placed on top of each other (as hydrograph overlays) on a light table, compared, and missing daily flow data estimated. This method, however, is subjective and can produce inconsistent results, because hydrographers can differ when calculating acceptable limits of deviation between observed and estimated flows. Selection of appropriate index stations also is judgemental, giving no consideration to the mathematical correlation between the review station and the index station(s).\r\n\r\n \r\n\r\nTo address the limitation of the hydrograph overlay method, a set of software programs, written in the SAS macrolanguage, was developed and designated Program HYDCOMP. The program automatically selects statistically comparable index stations by correlation and regression, and performs hydrographic comparisons and estimates of missing data by regressing daily mean flows at the review station against -8 to +8 lagged flows at one or two index stations and day-of-week. Another advantage that HYDCOMP has over the graphical method is that estimated flows, the criteria for determining the quality of the data, and the selection of index stations are determined statistically, and are reproducible from one user to another.\r\n\r\n \r\n\r\n HYDCOMP will load the most-correlated index stations into another file containing the ?best index stations,? but will not overwrite stations already in the file. A knowledgeable user should delete unsuitable index stations from this file based on standard error of estimate, hydrologic similarity of candidate index stations to the review station, and knowledge of the individual station characteristics. Also, the user can add index stations not selected by HYDCOMP, if desired.\r\n\r\n \r\n\r\nOnce the file of best-index stations is created, a user may do hydrographic comparison and data estimates by entering the number of the review station, selecting an index station, and specifying the periods to be used for regression and plotting. For example, the user can restrict the regression to ice-free periods of the year to exclude flows estimated during iced conditions. However, the regression could still be used to estimate flow during iced conditions.\r\n\r\n \r\n\r\nHYDCOMP produces the standard error of estimate as a measure of the central scatter of the regression and R-square (coefficient of determination) for evaluating the accuracy of the regression. Output from HYDCOMP includes plots of percent residuals against (1) time within the regression and plot periods, (2) month and day of the year for evaluating seasonal bias in the regression, and (3) the magnitude of flow. For hydrographic comparisons, it plots 2-month segments of hydrographs over the selected plot period showing the observed flows, the regressed flows, the 95 percent confidence limit flows, flow measurements, and regression limits. If the observed flows at the review station remain outside the 95 percent confidence limits for a prolonged period, there may be some error in the flows at the review station or at the index station(s). In addition, daily minimum and maximum temperatures and daily rainfall are shown on the hydrographs, if available, to help indicate whether an apparent change in flow may result from rainfall or from changes in backwater from melting ice or freezing water.\r\n\r\n \r\n\r\nHYDCOMP statistically smooths estimated flows from non-missing flows at the edges of the gaps in data into regressed flows at the center of the gaps using the Kalman smoothing algorithm. Missing flows are automatically estimated by HYDCOMP, but the user also can specify that periods of erroneous, but nonmissing flows, be estimated by the program.","language":"ENGLISH","doi":"10.3133/ofr02286","usgsCitation":"Sanders, C., 2002, Daily values flow comparison and estimates using program HYCOMP, version 1.0 (Version 1.0): U.S. Geological Survey Open-File Report 2002-286, iv, 52 p. : col. ill. ; 28 cm.; 4 refs, https://doi.org/10.3133/ofr02286.","productDescription":"iv, 52 p. : col. ill. ; 28 cm.; 4 refs","costCenters":[],"links":[{"id":176273,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":4317,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr02286/","linkFileType":{"id":5,"text":"html"}}],"edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e86a","contributors":{"authors":[{"text":"Sanders, Curtis L.","contributorId":94734,"corporation":false,"usgs":true,"family":"Sanders","given":"Curtis L.","affiliations":[],"preferred":false,"id":241626,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39942,"text":"wri024167 - 2002 - Hydrogeology, ground-water use, and ground-water levels in the Mill Creek Valley near Evendale, Ohio","interactions":[],"lastModifiedDate":"2019-04-17T08:19:42","indexId":"wri024167","displayToPublicDate":"2003-01-01T00:00:00","publicationYear":"2002","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2002-4167","displayTitle":"Hydrogeology, Ground-Water Use, and Ground-Water Levels in the Mill Creek Valley Near Evendale, Ohio","title":"Hydrogeology, ground-water use, and ground-water levels in the Mill Creek Valley near Evendale, Ohio","docAbstract":"Withdrawals of ground water in the central Mill Creek Valley near Evendale, Ohio, caused water-level declines of more than 100 feet by the 1950s. Since the 1950s, management practices have changed to reduce the withdrawals of ground water, and recovery of water levels in long-term monitoring wells in the valley has been documented. Changing conditions such as these prompted a survey of water use, streamflow conditions, and water levels in several aquifers in the central Mill Creek Valley, Hamilton and Butler Counties, Ohio. Geohydrologic information, water use, and water levels were compiled from historical records and collected during the regional survey. Data collected during the survey are presented in terms of updated geohydrologic information, water use in the study area, water levels in the aquifers, and interactions between ground water and surface water. Some of the data are concentrated at former Air Force Plant 36 (AFP36), which is collocated with the General Electric Aircraft Engines (GEAE) plant, and these data are used to describe geohydrology and water levels on a more local scale at and near the plant.
A comparison of past and current ground-water use and levels indicates that the demand for ground water is decreasing and water levels are rising. Before 1955, most of the major industrial ground-water users had their own wells, ground water was mined from a confined surficial (lower) aquifer, and water levels were more than 100 feet below their predevelopment level. Since 1955, however, these users have been purchasing their water from the city of Cincinnati or a private water purveyor. The cities of Reading and Lockland, both producers of municipal ground-water supplies in the area, shut down their well fields within their city limits. Because the demand for ground-water supplies in the valley has lessened greatly since the 1950s, withdrawals have decreased, and, consequently, water levels in the lower aquifer are 65 to 105 feet higher than they were in 1955.
During the time of the water-level survey (November 2000), ground water was being pumped from four locations in the lower aquifer, including three municipalities and one remediation site. Effects of pumping in those four areas were evident from the regional water-level data. Overall, the direction of ground-water flow in the lower aquifer is from northeast to southwest along the primary orientation of the Mill Creek Valley in the study area.
Water levels in shallower surficial aquifers were mapped at local scales centered on GEAE. Examination of well logs indicated that these aquifers (called shallow and water-table) are discontinuous and, on a regional scale, few wells were completed in these aquifers. Water levels in the shallow aquifer indicated that flow was from northeast to southwest except in areas where pumping in the lower aquifer or the proximity of Mill Creek may have been affecting water levels in the shallow aquifer. Water levels in the water-table aquifer indicated flow toward Mill Creek from GEAE.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024167","collaboration":"Prepared in cooperation with the U.S. Air Force Aeronautical Systems Center","usgsCitation":"Schalk, C., and Schumann, T., 2002, Hydrogeology, ground-water use, and ground-water levels in the Mill Creek Valley near Evendale, Ohio: U.S. Geological Survey Water-Resources Investigations Report 2002-4167, 33 p., https://doi.org/10.3133/wri024167.","productDescription":"33 p.","costCenters":[],"links":[{"id":165037,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4167/coverthb.jpg"},{"id":3640,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4167/wri20024167.pdf","text":"Report","size":"2.50 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRIR 2002-4167"}],"contact":"Director, Ohio Water Science Center
U.S. Geological Survey
6460 Busch Blvd.
Columbus, OH 43229
The U.S. Geological Survey, U.S. Environmental Protection Agency, and Illinois Environmental Protection Agency began a study of the hydrogeology, flow system, and distribution of contaminants in the aquifers underlying Belvidere, Ill., and vicinity in 1992. As part of the study, the ancestral Troy Bedrock Valley, located about 1.5 miles west of Belvidere, was identified as an important part of the ground-water-flow system. In the deepest parts of the valley, the basal Glenwood confining unit may be absent; thick deposits of sand and gravel that infill part of the valley may directly overlie the sandstone St. Peter aquifer, a regionally important source of water for public supply. With few deep wells open to the St. Peter aquifer present in the valley to provide necessary geologic information, tritium and other water-chemistry data were collected from eight wells to possibly delineate areas where the confining unit may be absent; the data also provide baseline water-quality information for an area expecting changes in land use and increases in water withdrawal. Also as part of the study, particle-tracking analysis was done using an available flow model to (1) identify possible discharge locations of ground water and contaminants and (2) delineate areas contributing recharge to the Belvidere municipal wells.
This report presents and interprets water-chemistry data collected during December 2000 and presents results of particle-tracking analysis. Ground water in samples from two of four wells open to the St. Peter aquifer appears to have recharged after 1954, suggesting that the Glenwood confining unit may be absent near the wells. Other hydrogeologic and water-chemistry data, however, were inconclusive or contradictory. Concentrations of iron, manganese, and lead exceeded maximum contaminant levels in five or less samples, but materials associated with the water-distribution systems appear to contribute to the elevated concentrations above natural levels.
Particle-tracking analysis indicates that most ground-water flow beneath possible contaminant-source areas discharges from the glacial drift aquifer to the Kishwaukee River. Most of the source areas are in or near Belvidere and are within 1,500 feet of the river. The analysis also indicates the possibility that in parts of the study area, some ground water does not discharge to the river, but flows beneath the Kishwaukee River in the underlying carbonate Galena-Platteville aquifer. Ground water that discharges to the one municipal well open to the glacial drift aquifer is estimated to travel over 1 mile in less than 25 years. Simulated residence (travel) times of ground water from the base of the glacial drift aquifer to the six municipal wells open, in part, to the Galena-Platteville aquifer, are estimated at less than about 40 years. Because fractures in this aquifer are unaccounted for in the flow model, actual areas contributing recharge are likely larger and travel times faster than those simulated for most of the municipal wells. Tritium data indicate that, in general, travel times from the land surface to the deepest parts of the Galena-Platteville aquifer are less than 46 years. Methyl tertiary-butyl ether data indicate that travel times to the upper part of the aquifer may be less than 16 years. The water-quality-based estimates of travel time generally are consistent with the estimates from particle-tracking analysis.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024062","collaboration":"Prepared in cooperation with the Illinois Environmental Protection Agency U.S. Environmental Protection Agency","usgsCitation":"Mills, P., Halford, K.J., and Cobb, R., 2002, Delineation of the Troy Bedrock Valley and particle-tracking analysis of ground-water flow underlying Belvidere, Illinois: U.S. Geological Survey Water-Resources Investigations Report 2002-4062, v, 46 p., https://doi.org/10.3133/wri024062.","productDescription":"v, 46 p.","costCenters":[{"id":344,"text":"Illinois Water Science Center","active":true,"usgs":true}],"links":[{"id":5984,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4062/wrir02_4062.pdf","text":"Report","size":"4.43 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRIR 02–4062"},{"id":183897,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4062/coverthb.jpg"}],"country":"United States","state":"Illinois","county":"Boone County","city":"Belvidere","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-88.9385,42.4984],[-88.7737,42.4958],[-88.7719,42.4957],[-88.7059,42.4972],[-88.705,42.4167],[-88.7041,42.329],[-88.7057,42.2418],[-88.7061,42.1564],[-88.8224,42.1557],[-88.94,42.1549],[-88.9406,42.2408],[-88.9405,42.3284],[-88.9392,42.4161],[-88.9385,42.4984]]]},\"properties\":{\"name\":\"Boone\",\"state\":\"IL\"}}]}","contact":"Director, Central Midwest Water Science Center
U.S. Geological Survey
405 North Goodwin
Urbana, IL 61801
In 1970, the Chester County Water Resources Authority (Pennsylvania) and the U.S. Geological Survey (USGS) established a longterm water-quality network with the goal of assessing the quality of streams in the county and understanding stream changes in response to urbanization using benthic-macroinvertebrate data. This database represents one of the longest continuous water-quality data sets in the country. Benthic macroinvertebrates are aquatic insects, such as mayflies, caddisflies, riffle beetles, and midges, and other invertebrates that live on the stream bottom. Benthic macroinvertebrates are useful in evaluating stream quality because their habitat preferences and low motility cause them to be affected directly by substances that enter the aquatic system. By evaluating the diversity and community structure of benthic-macroinvertebrate populations, a determination of stream quality can be made.
Between 1981 and 1997, the water-quality network consisted of 43 sites in 5 major basins in Chester County—Delaware, Schuylkill, Brandywine, Big Elk and Octoraro, and Red and White Clay. Benthicmacroinvertebrate, water-chemistry, and habitat data were collected each year in October or November during base-flow conditions. Using these data, Reif evaluated the overall water-quality condition of Chester County streams. This Fact Sheet summarizes the key findings from Reif for streams in the Brandywine Creek Basin. These streams include West Branch Brandywine Creek (sites 37 and 38), Buck Run (site 46), Doe Run (site 45), East Branch Brandywine Creek (sites 48, 42, 36, and 39), Indian Run (site 47), West Valley Creek (site 44), and Main Stem Brandywine Creek (site 40). This summary includes an analysis of stream conditions based on benthic-macroinvertebrate samples and an analysis of trends in stream conditions for the 17-year study period.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/fs11702","collaboration":"Prepared in cooperation with the Chester County Water Resources Authority","usgsCitation":"Reif, A.G., 2002, Assessment of stream quality using biological indices at selected sites in the Brandywine Creek basin, Chester County, Pennsylvania, 1981-97: U.S. Geological Survey Fact Sheet 117-02, 4 p., https://doi.org/10.3133/fs11702.","productDescription":"4 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":3746,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/2002/0117/fs20020117.pdf","text":"Report","size":"291 KB","linkFileType":{"id":1,"text":"pdf"},"description":"FS 2002-0117"},{"id":122027,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/2002/0117/coverthb.jpg"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
In 1970, the Chester County Water Resources Authority (Pennsylvania) and the U.S. Geological Survey (USGS) established a long-term water-quality network with the goal of assessing the quality of streams in the county and understanding stream changes in response to urbanization using benthic-macroinvertebrate data. This database represents one of the longest continuous water-quality data sets in the country. Benthic macroinvertebrates are aquatic insects, such as mayflies, caddisflies, riffle beetles, and midges, and other invertebrates that live on the stream bottom. Benthic macroinvertebrates are useful in evaluating stream quality because their habitat preference and low motility cause them to be affected directly by substances that enter the aquatic system. By evaluating the diversity and community structure of benthic-macroinvertebrate populations, a determination of stream quality can be made.
Between 1981 and 1997, the water-quality network consisted of 43 sites in 5 major basins in Chester County—Delaware, Schuylkill, Brandywine, Big Elk and Octoraro, and Red and White Clay. Benthicmacroinvertebrate, water-chemistry, and habitat data were collected each year in October or November during base-flow conditions. Using these data, Reif evaluates the overall water-quality condition of Chester County streams. This Fact Sheet summarizes the key findings from Reif for streams in the Red Clay and White Clay Creek Basins. These streams include East Branch Red Clay Creek (site 26), West Branch Red Clay Creek (site 27), East Branch White Clay Creek (site 28), the Middle Branch White Clay Creek (site 29), and West Branch White Clay Creek (site 30). This summary includes an analysis of stream conditions on the basis of benthic-macroinvertebrate samples and an analysis of trends in stream conditions for the 17-year study period.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/fs11802","collaboration":"Prepared in cooperation with the Chester County Water Resources Authority","usgsCitation":"Reif, A.G., 2002, Assessment of stream quality using biological indices at selected sites in the Red Clay and White Clay Creek basins, Chester County, Pennsylvania, 1981-97: U.S. Geological Survey Fact Sheet 118-02, 4 p., https://doi.org/10.3133/fs11802.","productDescription":"4 p.","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":3747,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/2002/0118/fs20020118.pdf","text":"Report","size":"278 KB","linkFileType":{"id":1,"text":"pdf"},"description":"FS 2002-0118"},{"id":120557,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/2002/0118/coverthb.jpg"}],"country":"United States","state":"Pennsylvania","county":"Chester","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-75.6968,40.2417],[-75.6912,40.2388],[-75.6894,40.2378],[-75.6864,40.2387],[-75.6784,40.2436],[-75.6741,40.2458],[-75.6705,40.2466],[-75.6645,40.2461],[-75.6549,40.2428],[-75.6478,40.2404],[-75.6406,40.2371],[-75.6304,40.2347],[-75.6209,40.2305],[-75.6186,40.2277],[-75.6151,40.2245],[-75.6114,40.2244],[-75.6078,40.2258],[-75.6047,40.2275],[-75.6059,40.2294],[-75.6076,40.2326],[-75.6088,40.2348],[-75.6081,40.2366],[-75.605,40.2389],[-75.6014,40.2379],[-75.5997,40.2365],[-75.5973,40.2347],[-75.591,40.2214],[-75.5835,40.21],[-75.5801,40.2045],[-75.5796,40.2004],[-75.5766,40.1981],[-75.5724,40.1967],[-75.5694,40.1966],[-75.5676,40.1975],[-75.5645,40.2006],[-75.5644,40.2029],[-75.5655,40.207],[-75.5661,40.2093],[-75.5636,40.2101],[-75.5606,40.2096],[-75.5589,40.2073],[-75.5554,40.2023],[-75.5503,40.19],[-75.544,40.1794],[-75.5387,40.1739],[-75.527,40.1664],[-75.5275,40.1492],[-75.5239,40.1468],[-75.5184,40.1475],[-75.5127,40.1595],[-75.503,40.1593],[-75.5,40.1563],[-75.5036,40.1506],[-75.5107,40.1422],[-75.5088,40.1347],[-75.4905,40.1253],[-75.4729,40.1287],[-75.4611,40.1241],[-75.4627,40.119],[-75.4691,40.1169],[-75.4719,40.1116],[-75.4693,40.1066],[-75.4618,40.1027],[-75.4633,40.0971],[-75.4563,40.0945],[-75.4558,40.0876],[-75.4401,40.0941],[-75.4369,40.0899],[-75.42,40.0966],[-75.3927,40.0604],[-75.3669,40.0723],[-75.361,40.0668],[-75.3702,40.062],[-75.3732,40.0602],[-75.3811,40.0572],[-75.4012,40.0475],[-75.4025,40.0471],[-75.4086,40.0436],[-75.4128,40.0418],[-75.4106,40.0373],[-75.4076,40.0336],[-75.406,40.0295],[-75.4139,40.0242],[-75.4207,40.0202],[-75.4311,40.0118],[-75.4508,39.9958],[-75.452,39.9949],[-75.4532,39.994],[-75.4521,39.9926],[-75.4455,39.9925],[-75.4437,39.9925],[-75.4412,39.9933],[-75.4401,39.9915],[-75.4372,39.9865],[-75.4385,39.9842],[-75.4398,39.9811],[-75.4399,39.9793],[-75.4423,39.9788],[-75.4446,39.9807],[-75.4726,39.968],[-75.4993,39.9557],[-75.5024,39.9544],[-75.5079,39.9518],[-75.5152,39.9483],[-75.5224,39.9452],[-75.5243,39.9443],[-75.5202,39.9397],[-75.5191,39.9374],[-75.5306,39.9322],[-75.526,39.9239],[-75.5315,39.9218],[-75.5366,39.9305],[-75.5427,39.9274],[-75.5398,39.9242],[-75.5447,39.922],[-75.5424,39.9183],[-75.5502,39.9152],[-75.5468,39.9093],[-75.5553,39.9058],[-75.5576,39.9086],[-75.5601,39.9072],[-75.5583,39.904],[-75.562,39.9023],[-75.5711,39.897],[-75.573,39.8943],[-75.5714,39.8879],[-75.5799,39.8835],[-75.5822,39.8854],[-75.5834,39.8849],[-75.5852,39.8863],[-75.5888,39.8846],[-75.5842,39.8804],[-75.5981,39.8747],[-75.5952,39.8724],[-75.5934,39.8697],[-75.5935,39.8683],[-75.5959,39.8652],[-75.599,39.862],[-75.6003,39.8602],[-75.6015,39.858],[-75.601,39.8562],[-75.5975,39.8539],[-75.5939,39.8515],[-75.5946,39.8488],[-75.5965,39.8457],[-75.5978,39.8416],[-75.5973,39.8379],[-75.6146,39.835],[-75.6308,39.8314],[-75.6464,39.827],[-75.647,39.8268],[-75.6661,39.82],[-75.6775,39.8156],[-75.6928,39.8074],[-75.7056,39.7991],[-75.7177,39.7912],[-75.724,39.7866],[-75.7268,39.7845],[-75.7378,39.775],[-75.7476,39.7653],[-75.7551,39.756],[-75.7611,39.7478],[-75.7662,39.7393],[-75.77,39.731],[-75.7723,39.7231],[-75.7875,39.7231],[-76.0148,39.7228],[-76.1392,39.7223],[-76.1373,39.7262],[-76.1337,39.728],[-76.1307,39.728],[-76.1266,39.7265],[-76.1236,39.7242],[-76.1188,39.726],[-76.1187,39.7301],[-76.1205,39.7333],[-76.1198,39.7364],[-76.1144,39.7368],[-76.1115,39.735],[-76.1121,39.7318],[-76.1134,39.7287],[-76.1104,39.7268],[-76.1051,39.7254],[-76.0996,39.7285],[-76.0965,39.7326],[-76.0959,39.7362],[-76.0988,39.738],[-76.1018,39.7399],[-76.1018,39.7421],[-76.1011,39.7449],[-76.0957,39.7448],[-76.0909,39.7452],[-76.0873,39.7474],[-76.0842,39.7537],[-76.0841,39.7592],[-76.0804,39.7609],[-76.0678,39.7626],[-76.066,39.7644],[-76.0654,39.7671],[-76.0659,39.7708],[-76.0628,39.7734],[-76.0616,39.7752],[-76.0615,39.7789],[-76.0567,39.7802],[-76.0537,39.7819],[-76.0506,39.7846],[-76.0481,39.79],[-76.0444,39.7963],[-76.0377,39.8026],[-76.0352,39.808],[-76.0303,39.813],[-76.0308,39.8175],[-76.032,39.8207],[-76.0265,39.8247],[-76.0253,39.826],[-76.0252,39.8301],[-76.0234,39.831],[-76.0191,39.8319],[-76.0191,39.8337],[-76.0202,39.8378],[-76.023,39.8464],[-76.0217,39.8518],[-76.0211,39.8537],[-76.0181,39.8545],[-76.0163,39.854],[-76.0127,39.8531],[-76.0103,39.8531],[-76.0091,39.8544],[-76.007,39.8666],[-76.0051,39.8712],[-76.0039,39.873],[-76.0015,39.8738],[-75.9991,39.8734],[-75.9974,39.8715],[-75.9956,39.8701],[-75.9932,39.8697],[-75.9926,39.8706],[-75.9908,39.8719],[-75.9877,39.8732],[-75.9871,39.8746],[-75.9877,39.8768],[-75.9912,39.8801],[-75.9905,39.8828],[-75.9899,39.8868],[-75.9879,39.8927],[-75.9885,39.895],[-75.9902,39.8977],[-75.9943,39.901],[-75.9961,39.9028],[-75.9957,39.9236],[-75.9962,39.9259],[-75.998,39.9273],[-75.9968,39.9282],[-75.9938,39.9277],[-75.9926,39.9268],[-75.9914,39.9272],[-75.9902,39.9286],[-75.9859,39.9308],[-75.9841,39.9308],[-75.9823,39.9307],[-75.9811,39.9316],[-75.9805,39.9334],[-75.9822,39.9362],[-75.9875,39.9399],[-75.9915,39.9481],[-75.9921,39.9513],[-75.992,39.9544],[-75.9901,39.958],[-75.9889,39.9607],[-75.987,39.9634],[-75.9869,39.9675],[-75.9722,39.9855],[-75.964,40.0008],[-75.9628,40.0026],[-75.956,40.0125],[-75.9504,40.0197],[-75.935,40.0394],[-75.9354,40.0471],[-75.9361,40.0689],[-75.9365,40.0807],[-75.9403,40.0989],[-75.9413,40.1066],[-75.9412,40.1093],[-75.9315,40.1138],[-75.9139,40.1212],[-75.9018,40.1261],[-75.8757,40.1371],[-75.8604,40.1464],[-75.8494,40.154],[-75.7773,40.1997],[-75.7724,40.2028],[-75.7602,40.2085],[-75.7322,40.2231],[-75.6986,40.2408],[-75.6968,40.2417]]]},\"properties\":{\"name\":\"Chester\",\"state\":\"PA\"}}]}","contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
Isotope data collected in the Calumet Region of northwestern Indiana and northeastern Illinois, one of the most heavily industrialized regions of the United States, indicated that water in the surficial Calumet aquifer is well mixed. The Calumet aquifer is recharged areally by precipitation and locally may be recharged by surface water. The residence time of ground water in the Calumet aquifer is approximately 5 to 15 years. Ground-water-flow rates through the Calumet aquifer are estimated to be 400 to 2,300 feet per year. The permeable deposits, shallow water table, lack of an overlying confining unit, and proximity to numerous contaminant sources indicate that the Calumet aquifer is vulnerable to contamination.
Isotopic data indicate that ground water in the confining unit underlying the Calumet aquifer is derived from a variety of sources that include Lake Michigan, modern precipitation, and discharge from the basal Silurian-Devonian bedrock aquifer. The source and apparent age of the water are variable and appear to be affected locally by various geologic and hydraulic factors. The vertical ground-water-flow rate through the unweathered part of the confining unit is about 0.20 feet per year and is about 6.3 feet per year through the weathered part. The data indicate the weathered part of the confining unit may be more vulnerable to contamination than the unweathered confining unit.
Ground water in the basal Silurian-Devonian aquifer is derived from Lake Michigan, glacial-age water, and modern precipitation. Post-1952 recharge has occurred in the vicinity of Stony Island, Ill. Ground-water recharge of the Silurian-Devonian aquifer may be occurring near Calumet Harbor. The Silurian-Devonian aquifer is vulnerable to contamination where the confining unit is thin or absent or where the integrity of the confining unit has been compromised.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri024213","usgsCitation":"Kay, R.T., Bayless, E.R., and Solak, R.A., 2002, Use of isotopes to identify sources of ground water, estimate ground-water-flow rates, and assess aquifer vulnerability in the Calumet region of northwestern Indiana and northeastern Illinois: U.S. Geological Survey Water-Resources Investigations Report 2002-4213, v, 60 p., https://doi.org/10.3133/wri024213.","productDescription":"v, 60 p.","numberOfPages":"70","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":407654,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_53971.htm","linkFileType":{"id":5,"text":"html"}},{"id":135956,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4213/coverthb.jpg"},{"id":3935,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4213/wri20024213.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2002-4213"}],"country":"United States","state":"Illinois, Indiana","otherGeospatial":"Calumut region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.7333,\n 41.5589\n ],\n [\n -87.0833,\n 41.5589\n ],\n [\n -87.0833,\n 41.7472\n ],\n [\n -87.7333,\n 41.7472\n ],\n [\n -87.7333,\n 41.5589\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, Indiana Water Science Center
U.S. Geological Survey
5957 Lakeside Blvd.
Indianapolis, IN 46278
Director, New Mexico Water Science Center
U.S. Geological Survey
6700 Edith Blvd NE
Albuquerque, NM 87113
The Kansas State Legislature, by enacting Kansas Statute KSA 82a-2001 et. seq., mandated the criteria for determining which Kansas stream segments would be subject to classification by the State. One criterion for the selection as a classified stream segment is based on the statistic of median flow being equal to or greater than 1 cubic foot per second. As specified by KSA 82a-2001 et. seq., median flows were determined from U.S. Geological Survey streamflow-gaging-station data by using the most-recent 10-years of gaged data (KSA) for each streamflow-gaging station. Median flows also were determined by using gaged data from the entire period of record (all-available hydrology, AAH).
Least-squares multiple regression techniques were used, along with Tobit analyses, to develop equations for estimating median flows for uncontrolled stream segments. The drainage area of the uncontrolled gaging stations used in the regression analyses ranged from 2.06 to 12,004 square miles. A logarithmic transformation of the data was needed to develop the best linear relation for computing median flows. In the regression analyses, the significant climatic and basin characteristics, in order of importance, were drainage area, mean annual precipitation, mean basin permeability, and mean basin slope. Tobit analyses of KSA data yielded a root mean square error of 0.285 logarithmic units, and the best equations using Tobit analyses of AAH data had a root mean square error of 0.247 logarithmic units.
These equations and an interpolation procedure were used to compute median flows for the uncontrolled stream segments on the Kansas Surface Water Register. Measured median flows from gaging stations were incorporated into the regression-estimated median flows along the stream segments where available. The segments that were uncontrolled were interpolated using gaged data weighted according to the drainage area and the bias between the regression-estimated and gaged flow information. On controlled reaches of Kansas streams, the median flow information was interpolated between gaging stations using only gaged data weighted by drainage area.
Of the 2,232 total stream segments on the Kansas Surface Water Register, 30 percent of the segments had an estimated median streamflow of less than 1 cubic foot per second when the KSA analysis was used. When the AAH analysis was used, 40 percent of the segments had an estimated median streamflow of less than 1 cubic foot per second.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri20024292","collaboration":"Prepared in cooperation with the Kansas Department of Health and Environment","usgsCitation":"Perry, C.A., Wolock, D.M., and Artman, J.C., 2002, Estimates of median flows for streams on the Kansas surface water register (Superseded by SIR 2004-5032): U.S. Geological Survey Water-Resources Investigations Report 2002-4292, vi, 107 p., https://doi.org/10.3133/wri20024292.","productDescription":"vi, 107 p.","numberOfPages":"114","costCenters":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"links":[{"id":360235,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2002/4292/wrir20024292.pdf","text":"Report","size":"29.0 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRIR 2002–4292"},{"id":134549,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2002/4292/coverthb.jpg"}],"country":"United States","state":"Kansas","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-99.541116,36.999573],[-99.648652,36.999604],[-99.657658,37.000197],[-99.875409,37.001659],[-99.995201,37.001631],[-100.115722,37.002206],[-100.193754,37.002133],[-100.552683,37.000735],[-100.734517,36.999059],[-100.756894,36.999357],[-100.855634,36.998626],[-100.904274,36.998745],[-100.945469,36.998153],[-101.012641,36.998176],[-101.359674,36.996232],[-102.04224,36.993083],[-102.041749,37.034397],[-102.041809,37.111973],[-102.042092,37.125021],[-102.041963,37.258164],[-102.041664,37.29765],[-102.042089,37.352819],[-102.041524,37.375018],[-102.042016,37.535261],[-102.041574,37.680436],[-102.042158,37.760164],[-102.042953,37.803535],[-102.044644,38.045532],[-102.044255,38.113011],[-102.044589,38.125013],[-102.044251,38.141778],[-102.044944,38.384419],[-102.044442,38.415802],[-102.044936,38.41968],[-102.045324,38.453647],[-102.045074,38.669617],[-102.045334,38.799463],[-102.046571,39.047038],[-102.04937,39.41821],[-102.049554,39.538932],[-102.050422,39.646048],[-102.050099,39.653812],[-102.050594,39.675594],[-102.051569,39.849805],[-102.051744,40.003078],[-101.904176,40.003162],[-101.841025,40.002784],[-101.409953,40.002354],[-101.324036,40.002696],[-100.937427,40.002145],[-100.75883,40.002302],[-100.66023,40.002162],[-100.645445,40.001883],[-100.196959,40.001494],[-99.990926,40.001503],[-99.948167,40.001813],[-99.930433,40.001516],[-99.813401,40.0014],[-99.772121,40.001804],[-99.756835,40.001342],[-99.746628,40.00182],[-99.49766,40.001912],[-99.423565,40.00227],[-99.412645,40.001868],[-99.282967,40.001879],[-99.018701,40.002333],[-98.710404,40.00218],[-98.690287,40.002548],[-98.652494,40.002245],[-98.64071,40.002493],[-98.560578,40.002274],[-98.274017,40.002516],[-98.250008,40.002307],[-98.193483,40.002614],[-98.099659,40.002227],[-97.838379,40.00191],[-97.777155,40.002167],[-97.510264,40.001835],[-97.369199,40.00206],[-97.20231,40.001442],[-97.142448,40.001495],[-97.137866,40.001814],[-97.049663,40.001323],[-96.916093,40.001506],[-96.622401,40.001158],[-96.610349,40.000881],[-96.467536,40.001035],[-96.125937,40.000432],[-96.02409,40.000719],[-95.30829,39.999998],[-95.308404,39.993758],[-95.30778,39.990618],[-95.307111,39.989114],[-95.302507,39.984357],[-95.289715,39.977706],[-95.274757,39.972115],[-95.269886,39.969396],[-95.261854,39.960618],[-95.257652,39.954886],[-95.250254,39.948644],[-95.241383,39.944949],[-95.236761,39.943931],[-95.231114,39.943784],[-95.220212,39.944433],[-95.21644,39.943953],[-95.213737,39.943206],[-95.204428,39.938949],[-95.201277,39.934194],[-95.20069,39.928155],[-95.20201,39.922438],[-95.205745,39.915169],[-95.206326,39.912121],[-95.206196,39.909557],[-95.205733,39.908275],[-95.201935,39.904053],[-95.199347,39.902709],[-95.193816,39.90069],[-95.189565,39.899959],[-95.179453,39.900062],[-95.172296,39.902026],[-95.159834,39.906984],[-95.156024,39.907243],[-95.149657,39.905948],[-95.146055,39.904183],[-95.143802,39.901918],[-95.142563,39.897992],[-95.142445,39.89542],[-95.143403,39.889356],[-95.142718,39.885889],[-95.140601,39.881688],[-95.137092,39.878351],[-95.134747,39.876852],[-95.128166,39.874165],[-95.105912,39.869164],[-95.090158,39.86314],[-95.085003,39.861883],[-95.081534,39.861718],[-95.052535,39.864374],[-95.042142,39.864805],[-95.037767,39.865542],[-95.032053,39.868337],[-95.027931,39.871522],[-95.025422,39.876711],[-95.025119,39.878833],[-95.025947,39.886747],[-95.02524,39.8897],[-95.024389,39.891202],[-95.018743,39.897372],[-95.013152,39.899953],[-95.00844,39.900596],[-95.003819,39.900401],[-94.990284,39.89701],[-94.986975,39.89667],[-94.977749,39.897472],[-94.963345,39.901136],[-94.959276,39.901671],[-94.95154,39.900533],[-94.943867,39.89813],[-94.934493,39.893366],[-94.929574,39.888754],[-94.927897,39.886112],[-94.927359,39.883966],[-94.927252,39.880258],[-94.928466,39.876344],[-94.931463,39.872602],[-94.938791,39.866954],[-94.940743,39.86441],[-94.942407,39.861066],[-94.942567,39.856602],[-94.939767,39.85193],[-94.937655,39.849786],[-94.92615,39.841322],[-94.916918,39.836138],[-94.909942,39.834426],[-94.903157,39.83385],[-94.892677,39.834378],[-94.889493,39.834026],[-94.886933,39.833098],[-94.881013,39.828922],[-94.878677,39.826522],[-94.877044,39.823754],[-94.876544,39.820594],[-94.875944,39.813294],[-94.876344,39.806894],[-94.880932,39.797338],[-94.884084,39.794234],[-94.890292,39.791626],[-94.892965,39.791098],[-94.925605,39.789754],[-94.929654,39.788282],[-94.932726,39.786282],[-94.935206,39.78313],[-94.935782,39.778906],[-94.935302,39.77561],[-94.934262,39.773642],[-94.929653,39.769098],[-94.926229,39.76649],[-94.916789,39.760938],[-94.912293,39.759338],[-94.906244,39.759418],[-94.899156,39.761258],[-94.895268,39.76321],[-94.883924,39.770186],[-94.88146,39.771258],[-94.871144,39.772994],[-94.869644,39.772894],[-94.867143,39.771694],[-94.865243,39.770094],[-94.863143,39.767294],[-94.860743,39.763094],[-94.859443,39.753694],[-94.860371,39.74953],[-94.862943,39.742994],[-94.870143,39.734594],[-94.875643,39.730494],[-94.884143,39.726794],[-94.891744,39.724894],[-94.899316,39.724042],[-94.902612,39.724202],[-94.910068,39.725786],[-94.918324,39.728794],[-94.930005,39.73537],[-94.939221,39.741578],[-94.944741,39.744377],[-94.948726,39.745593],[-94.95263,39.745961],[-94.955286,39.745689],[-94.960086,39.743065],[-94.965318,39.739065],[-94.970422,39.732121],[-94.971206,39.729305],[-94.971078,39.723146],[-94.968453,39.707402],[-94.968981,39.692954],[-94.969909,39.68905],[-94.971317,39.68641],[-94.976325,39.68137],[-94.981557,39.678634],[-94.984149,39.67785],[-94.993557,39.67657],[-95.001379,39.676479],[-95.009023,39.675765],[-95.01531,39.674262],[-95.018318,39.672869],[-95.024595,39.668485],[-95.027644,39.665454],[-95.037464,39.652905],[-95.039049,39.649639],[-95.044554,39.64437],[-95.049518,39.637876],[-95.053367,39.630347],[-95.054925,39.624995],[-95.055152,39.621657],[-95.053012,39.613965],[-95.047911,39.606288],[-95.046445,39.601606],[-95.046361,39.599557],[-95.047165,39.595117],[-95.049277,39.589583],[-95.054804,39.582488],[-95.056897,39.580567],[-95.059519,39.579132],[-95.064519,39.577115],[-95.069315,39.576218],[-95.07216,39.576122],[-95.076688,39.576764],[-95.089515,39.581028],[-95.095736,39.580618],[-95.099095,39.579691],[-95.103228,39.577783],[-95.106406,39.575252],[-95.107454,39.573843],[-95.113077,39.559133],[-95.113557,39.553941],[-95.109304,39.542285],[-95.106596,39.537657],[-95.102888,39.533347],[-95.092704,39.524241],[-95.082714,39.516712],[-95.077441,39.513552],[-95.059461,39.506143],[-95.05638,39.503972],[-95.052177,39.499996],[-95.050552,39.497514],[-95.049845,39.494415],[-95.04837,39.48042],[-95.047133,39.474971],[-95.045716,39.472459],[-95.04078,39.466387],[-95.0375,39.463689],[-95.033408,39.460876],[-95.028498,39.458287],[-95.015825,39.452809],[-94.995768,39.448174],[-94.990172,39.446192],[-94.982144,39.440552],[-94.978798,39.436241],[-94.976606,39.426701],[-94.972952,39.421705],[-94.966066,39.417288],[-94.954817,39.413844],[-94.951209,39.411707],[-94.947864,39.408604],[-94.946293,39.405646],[-94.946662,39.399717],[-94.946227,39.395648],[-94.945577,39.393851],[-94.942039,39.389499],[-94.937158,39.386531],[-94.933652,39.385546],[-94.92311,39.384492],[-94.919225,39.385174],[-94.915859,39.386348],[-94.909581,39.388865],[-94.901823,39.392798],[-94.894979,39.393565],[-94.891845,39.393313],[-94.888972,39.392432],[-94.885026,39.389801],[-94.880979,39.383899],[-94.879281,39.37978],[-94.879088,39.375703],[-94.88136,39.370383],[-94.885216,39.366911],[-94.890928,39.364031],[-94.896832,39.363135],[-94.899024,39.362431],[-94.902497,39.360383],[-94.907297,39.356735],[-94.909409,39.354255],[-94.910017,39.352543],[-94.910641,39.348335],[-94.908065,39.323663],[-94.905329,39.311952],[-94.903137,39.306272],[-94.900049,39.300192],[-94.895217,39.294208],[-94.887056,39.28648],[-94.882576,39.283328],[-94.87832,39.281136],[-94.867568,39.277841],[-94.857072,39.273825],[-94.84632,39.268481],[-94.837855,39.262417],[-94.831471,39.256273],[-94.827487,39.249889],[-94.825663,39.241729],[-94.826111,39.238289],[-94.827791,39.234001],[-94.834896,39.223842],[-94.835056,39.220658],[-94.833552,39.217794],[-94.831679,39.215938],[-94.823791,39.209874],[-94.820687,39.208626],[-94.811663,39.206594],[-94.799663,39.206018],[-94.787343,39.207666],[-94.783838,39.207154],[-94.781518,39.206146],[-94.777838,39.203522],[-94.775543,39.200609],[-94.770338,39.190002],[-94.763138,39.179903],[-94.752338,39.173203],[-94.741938,39.170203],[-94.736537,39.169203],[-94.723637,39.169003],[-94.714137,39.170403],[-94.696332,39.178563],[-94.687236,39.183503],[-94.680336,39.184303],[-94.669135,39.182003],[-94.663835,39.179103],[-94.660315,39.168051],[-94.662435,39.157603],[-94.650735,39.154103],[-94.640035,39.153103],[-94.623934,39.156603],[-94.615834,39.160003],[-94.608834,39.160503],[-94.601733,39.159603],[-94.596033,39.157703],[-94.591933,39.155003],[-94.589933,39.140403],[-94.592533,39.135903],[-94.600434,39.128503],[-94.605734,39.122204],[-94.607034,39.119404],[-94.607354,39.113444],[-94.607234,39.065704],[-94.608334,38.981806],[-94.608134,38.940006],[-94.607866,38.937398],[-94.608033,38.847207],[-94.607625,38.82756],[-94.611602,38.635384],[-94.611465,38.625011],[-94.611858,38.620485],[-94.611887,38.580139],[-94.612176,38.576546],[-94.612157,38.549817],[-94.613365,38.403422],[-94.613312,38.364407],[-94.612673,38.314832],[-94.612658,38.217649],[-94.613856,38.149769],[-94.614212,37.992462],[-94.614465,37.987799],[-94.614612,37.944362],[-94.617721,37.77297],[-94.617975,37.722176],[-94.617651,37.687671],[-94.617885,37.682214],[-94.616789,37.52151],[-94.618505,37.181184],[-94.617875,37.056798],[-94.61808,36.998135],[-94.625224,36.998672],[-94.83128,36.998812],[-95.049499,36.99958],[-95.80798,36.999124],[-95.91018,36.999336],[-96.00081,36.99886],[-96.394272,36.999221],[-96.500288,36.998643],[-96.73659,36.999286],[-96.749838,36.998988],[-96.79206,36.99918],[-96.795199,36.99886],[-96.822791,36.999182],[-96.87629,36.999233],[-97.46228,36.998685],[-97.606549,36.998682],[-97.637137,36.99909],[-98.219499,36.997824],[-98.354073,36.997961],[-98.408991,36.998513],[-98.544872,36.998997],[-98.714512,36.99906],[-98.761597,36.999425],[-98.880009,36.999263],[-99.029337,36.999595],[-99.049695,36.999221],[-99.277506,36.999579],[-99.375391,37.000177],[-99.407015,36.999579],[-99.541116,36.999573]]]},\"properties\":{\"name\":\"Kansas\",\"nation\":\"USA \"}}]}","edition":"Superseded by SIR 2004-5032","contact":"Director, Kansas Water Science Center
U.S. Geological Survey
1217 Biltmore Drive
Lawrence, KS 66049
Data on the construction characteristics and the composition of influent and effluent at 13 underground, limestone-filled drains in Pennsylvania and Maryland are reported to evaluate the design and performance of limestone drains for the attenuation of acidity and dissolved metals in acidic mine drainage. On the basis of the initial mass of limestone, dimensions of the drains, and average flow rates, the initial porosity and average detention time for each drain were computed. Calculated porosity ranged from 0.12 to 0.50 with corresponding detention times at average flow from 1.3 to 33 h. The effectiveness of treatment was dependent on influent chemistry, detention time, and limestone purity. At two sites where influent contained elevated dissolved Al (>5 mg/liter), drain performance declined rapidly; elsewhere the drains consistently produced near-neutral effluent, even when influent contained small concentrations of dissolved Fe^+ (<5 mg/liter). Rates of limestone dissolution computed on the basis of average long-term Ca ion flux normalized by initial mass and purity of limestone at each of the drains ranged from 0.008 to 0.079 year-1. Data for alkalinity concentration and flux during 11-day closed-container tests using an initial mass of 4kg crushed limestone and a solution volume of 2.3 liter yielded dissolution rate constants that were comparable to these long-term field rates. An analytical method is proposed using closed-container test data to evaluate long-term performance (longevity) or to estimate the mass of limestone needed for a limestone treatment. This method condisers flow rate, influent alkalinity, steady-state alkalinity of effluent, and desired effluent alkalinity or detention time at a future time(s) and aplies first-order rate laws for limestone dissolution (continuous) and production of alkalinity (bounded).