No abstract available.
","language":"English","publisher":"United States Geological Survey","doi":"10.3133/ofr00358","issn":"0094-9140","usgsCitation":"Poppe, L., and Polloni, C.F., 2000, USGS East-Coast sediment analysis: Procedures, database, and georeferenced displays: U.S. Geological Survey Open-File Report 2000-358, HTML Document; CD-ROM, https://doi.org/10.3133/ofr00358.","productDescription":"HTML Document; CD-ROM","costCenters":[],"links":[{"id":391123,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34837.htm"},{"id":154420,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":1332,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/of00-358/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","otherGeospatial":"East Coast","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -68.02734375,\n 45.9511496866914\n ],\n [\n -82.265625,\n 37.16031654673677\n ],\n [\n -87.5390625,\n 31.952162238024975\n ],\n [\n -91.58203125,\n 28.613459424004414\n ],\n [\n -80.15625,\n 24.686952411999155\n ],\n [\n -79.62890625,\n 31.052933985705163\n ],\n [\n -74.1796875,\n 37.996162679728116\n ],\n [\n -67.32421875,\n 42.94033923363181\n ],\n [\n -67.1484375,\n 44.59046718130883\n ],\n [\n -68.02734375,\n 45.9511496866914\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a28e4b07f02db610e73","contributors":{"authors":[{"text":"Poppe, Lawrence J. lpoppe@usgs.gov","contributorId":2149,"corporation":false,"usgs":true,"family":"Poppe","given":"Lawrence J.","email":"lpoppe@usgs.gov","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":187762,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Polloni, C. F.","contributorId":13618,"corporation":false,"usgs":true,"family":"Polloni","given":"C.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":187763,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":26811,"text":"wri004279 - 2000 - Shoals and valley plugs in the Hatchie River watershed","interactions":[],"lastModifiedDate":"2012-02-02T00:08:33","indexId":"wri004279","displayToPublicDate":"2001-09-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4279","title":"Shoals and valley plugs in the Hatchie River watershed","docAbstract":"Agricultural land use and gully erosion have historically contributed more sediment to the streams of the Hatchie River watershed than those streams can carry. In 1970, the main sedimentation problem in the watershed occurred in the tributary flood plains. This problem motivated channelization projects (U.S. Department of Agriculture, 1970). By the mid-1980's, concern had shifted to sedimentation in the Hatchie River itself where channelized tributaries were understood to contribute much of the sediment. The Soil Conservation Service [Natural Resources Conservation Service (NRCS) since 1996] estimated that 640,000 tons of bedload (sand) accumulates in the Hatchie River each year and identified roughly the eastern two-thirds of the watershed, where loess is thin or absent, as the main source of sand (U.S. Department of Agriculture, 1986a). The U.S. Geological Survey (USGS), in cooperation with the West Tennessee River Basin Authority (WTRBA), conducted a study of sediment accumulation in the Hatchie River and its tributaries. This report identifies the types of tributaries and evaluates sediment, shoal formation, and valley-plug problems. The results presented here may contribute to a better understanding of similar problems in West Tennessee and the rest of the southeastern coastal plain. This information also will help the WTRBA manage sedimentation and erosion problems in the Hatchie River watershed.The source of the Mississippi section of the Hatchie River is in the sand hills southwest of Corinth, Mississippi (fig. 1). This section of the Hatchie River flows northward in an artificial drainage canal, gathering water from tributary streams that also are channelized. The drainage canal ends 2 miles south of the Tennessee State line. The Tennessee section of the Hatchie River winds north and west in a meandering natural channel to the Mississippi River. Although most of the Hatchie River tributaries are also drainage canals, the river's main stem has kept most of its natural character. The Hatchie River flows through a wide valley bottom occupied mostly by riverine wetland. Historically, the valley bottom has supported hardwood forests. Since publication of the first Hatchie River report (U.S. Department of Agriculture, 1970), the channel of the river has become shallower, and flooding has increased (U.S. Department of Agriculture 1986b). These wetter conditions inhibit growth of hardwoods and lead to premature hardwood mortality. The NRCS has predicted that despite efforts to control erosion in the uplands, most of the valley-bottom forest will die. '...swamping may be so prevalent as to change most of the Hatchie River Basin flood plain into a marsh condition, with the only remnants of the present bottomland hardwood timber remaining. (U.S. Department of Agriculture, 1986b) Loss of channel depth has been concentrated in short reaches near tributary mouths. At the mouths of Richland, Porters, Clover, and Muddy Creeks, navigation has become difficult for recreational users (Johnny Carlin, West Tennessee River Basin Authority, oral commun., 1998).As the low-gradient alluvial system of the Hatchie River accumulates sediment, another common outcome has been the formation of valley plugs, areas where 'channels are filled with sediment, and all the additional bedload brought downstream is then spread out over the flood plain until a new channel has been formed' (Happ, 1975). Valley plugs typically form where the slope of a sand-laden tributary decreases downstream, or where the tributary joins its parent stream (Happ and others, 1940; Diehl, 1994, 1997; Smith and Diehl, 2000). ","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri004279","usgsCitation":"Diehl, T.H., 2000, Shoals and valley plugs in the Hatchie River watershed: U.S. Geological Survey Water-Resources Investigations Report 2000-4279, 1 folded sheet; 8 p. :col. ill., col. maps ;28 cm., https://doi.org/10.3133/wri004279.","productDescription":"1 folded sheet; 8 p. :col. ill., col. maps ;28 cm.","costCenters":[],"links":[{"id":158419,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2095,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004279","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f8e4b07f02db5f2695","contributors":{"authors":[{"text":"Diehl, Timothy H. 0000-0001-9691-2212 thdiehl@usgs.gov","orcid":"https://orcid.org/0000-0001-9691-2212","contributorId":546,"corporation":false,"usgs":true,"family":"Diehl","given":"Timothy","email":"thdiehl@usgs.gov","middleInitial":"H.","affiliations":[{"id":581,"text":"Tennessee Water Science Center","active":true,"usgs":true},{"id":24708,"text":"Lower Mississippi-Gulf Water Science Center","active":true,"usgs":true}],"preferred":true,"id":197048,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":29968,"text":"wri004130 - 2000 - Trends in precipitation and streamflow and changes in stream morphology in the Fountain Creek watershed, Colorado, 1939-99","interactions":[],"lastModifiedDate":"2022-09-19T18:37:44.271355","indexId":"wri004130","displayToPublicDate":"2001-08-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4130","title":"Trends in precipitation and streamflow and changes in stream morphology in the Fountain Creek watershed, Colorado, 1939-99","docAbstract":"The Fountain Creek watershed, located in and along the eastern slope of the Front Range section of the southern Rocky Mountains, drains approximately 930 square miles of parts of Teller, El Paso, and Pueblo Counties in eastern Colorado. Streamflow in the watershed is dominated by spring snowmelt runoff and storm runoff during the summer monsoon season. Flooding during the 1990?s has resulted in increased streambank erosion. Property loss and damage associated with flooding and bank erosion has cost area residents, businesses, utilities, municipalities, and State and Federal agencies millions of dollars. Precipitation (4 stations) and streamflow (6 stations) data, aerial photographs, and channel reconnaissance were used to evaluate trends in precipitation and streamflow and changes in channel morphology. Trends were evaluated for pre-1977, post-1976, and period-of-record time periods. Analysis revealed the lack of trend in total annual and seasonal precipitation during the pre-1977 time period. In general, the analysis also revealed the lack of trend in seasonal precipitation for all except the spring season during the post-1976 time period. Trend analysis revealed a significant upward trend in long-term (period of record) total annual and spring precipitation data, apparently due to a change in total annual precipitation throughout the Fountain Creek watershed. During the pre-1977 time period, precipitation was generally below average; during the post- 1976 time period, total annual precipitation was generally above average. During the post- 1976 time period, an upward trend in total annual and spring precipitation was indicated at two stations. Because two of four stations evaluated had upward trends for the post-1976 period and storms that produce the most precipitation are isolated convection storms, it is plausible that other parts of the watershed had upward precipitation trends that could affect trends in streamflow. Also, because of the isolated nature of convection storms that hit some areas of the watershed and not others, it is difficult to draw strong conclusions on relations between streamflow and precipitation. Trends in annual instantaneous peak streamflow, 70th percentile, 90th percentile, maximum daily-mean streamflow (100th percentile), 7-, 14-, and 30-day high daily-mean stream- flow duration, minimum daily-mean streamflow (0th percentile), 10th percentile, 30th percentile, and 7-, 14-, 30-day low daily-mean streamflow duration were evaluated. In general, instantaneous peak streamflow has not changed significantly at most of the stations evaluated. Trend analysis revealed the lack of a significant upward trend in streamflow at all stations for the pre-1977 time period. Trend tests indicated a significant upward trend in high and low daily-mean streamflow statistics for the post-1976 period. Upward trends in high daily-mean streamflow statistics may be an indication that changes in land use within the watershed have increased the rate and magnitude of runoff. Upward trends in low daily-mean 2 Trends in Precipitation and Streamflow and Changes in Stream Morphology in the Fountain Creek Watershed, Colorado, 1939-99 streamflow statistics may be related to changes in water use and management. An analysis of the relation between streamflow and precipitation indicated that changes in water management have had a marked effect on streamflow. Observable change in channel morphology and changes in distribution and density of vegetation varied with magnitude, duration, and frequency of large streamflow events, and increases in the magnitude and duration of low streamflows. Although more subtle, low stream- flows were an important component of day-to-day channel erosion. Substantial changes in channel morphology were most often associated with infrequent large or catastrophic streamflow events that erode streambed and banks, alter stream course, and deposit large amounts of sediment in the flood plain.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004130","usgsCitation":"Stogner, 2000, Trends in precipitation and streamflow and changes in stream morphology in the Fountain Creek watershed, Colorado, 1939-99: U.S. Geological Survey Water-Resources Investigations Report 2000-4130, v, 43 p., https://doi.org/10.3133/wri004130.","productDescription":"v, 43 p.","costCenters":[],"links":[{"id":160489,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":406992,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_33858.htm","linkFileType":{"id":5,"text":"html"}},{"id":2433,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri00-4130","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Colorado","otherGeospatial":"Fountain Creek watershed","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105,\n 38.264\n ],\n [\n -104.5,\n 38.264\n ],\n [\n -104.5,\n 39.083\n ],\n [\n -105,\n 39.083\n ],\n [\n -105,\n 38.264\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625a60","contributors":{"authors":[{"text":"Stogner 0000-0002-3185-1452 rstogner@usgs.gov","orcid":"https://orcid.org/0000-0002-3185-1452","contributorId":938,"corporation":false,"usgs":true,"family":"Stogner","email":"rstogner@usgs.gov","affiliations":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"preferred":false,"id":202452,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":31169,"text":"ofr00351 - 2000 - Geologic map and database of the Salem East and Turner 7.5 minute quadrangles, Marion County, Oregon: A digital database","interactions":[],"lastModifiedDate":"2022-02-01T20:18:19.696676","indexId":"ofr00351","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2000-351","title":"Geologic map and database of the Salem East and Turner 7.5 minute quadrangles, Marion County, Oregon: A digital database","docAbstract":"The Salem East and Turner 7.5-minute quadrangles are situated in the center of the Willamette Valley near the western margin of the Columbia River Basalt Group (CRBG) distribution. The terrain within the area is of low to moderate relief, ranging from about 150 to almost 1,100-ft elevation. Mill Creek flows northward from the Stayton basin (Turner quadrangle) to the northern Willamette Valley (Salem East quadrangle) through a low that dissects the Columbia River basalt that forms the Salem Hills on the west and the Waldo Hills to the east. Approximately eight flows of CRBG form a thickness of up to 700 in these two quadrangles. The Ginkgo intracanyon flow that extends from east to west through the south half of the Turner quadrangle is exposed in the hills along the southeast part of the quadrangle.
Previous geologic mapping by Thayer (1939) and Bela (1981) while providing the general geologic framework did not subdivide the CRBG which limited their ability to delineate structural elements. Reconnaissance mapping of the CRBG units in the Willamette Valley indicated that these stratigraphic units could serve as a series of unique reference horizons for identifying post-Miocene folding and faulting (Beeson and others, 1985,1989; Beeson and Tolan, 1990). Crenna, et al. (1994) compiled previous mapping in the Willamette Valley in a study of the tectonics of the Salem area.
The major emphasis of this study was to identify and map CRBG units within the Salem East and Turner Quadrangles and to utilize this detailed CRBG stratigraphy to identify and characterize structural features. Water well logs were used to provide better subsurface stratigraphic control. Three other quadrangles (Scotts Mills, Silverton, and Stayton NE) in the Willamette Valley have been mapped in this way (Tolan and Beeson, 1999).
This area was a lowland area of weathered and eroded marine sedimentary when the Columbia River basalts encroached on this area approximately 15-16 m.y. ago. An incipient Coast Range apparently stopped or diverted the fluid lava flows from moving much farther westward toward the coast at this latitude. It is assumed also that an ancestral Willamette River flowed northward through this low-lying area so that water was present as streams and ponds along the flood plain.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr00351","usgsCitation":"Tolan, T.L., Beeson, M.H., and DuRoss, C., 2000, Geologic map and database of the Salem East and Turner 7.5 minute quadrangles, Marion County, Oregon: A digital database: U.S. Geological Survey Open-File Report 2000-351, 2 Plates: 30.93 x 35.04 inches and 31.73 x 35.20 inches; Readme, https://doi.org/10.3133/ofr00351.","productDescription":"2 Plates: 30.93 x 35.04 inches and 31.73 x 35.20 inches; Readme","additionalOnlineFiles":"Y","costCenters":[{"id":412,"text":"National Cooperative Geologic Mapping Program","active":false,"usgs":true}],"links":[{"id":161020,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr00351.gif"},{"id":2676,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/0351/","linkFileType":{"id":5,"text":"html"}},{"id":281611,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2000/0351/00351ps.tar.gz"},{"id":281612,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2000/0351/00351db.tar.gz"},{"id":281613,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2000/0351/00351db.zip"},{"id":281614,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/of/2000/0351/pdf/README.PDF"},{"id":281610,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2000/0351/pdf/tnrfinal.pdf"},{"id":281615,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2000/0351/pdf/slmfinal.pdf"},{"id":110130,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34045.htm","linkFileType":{"id":5,"text":"html"},"description":"34045"}],"scale":"24000","projection":"Universal Transverse Mercator projection","country":"United States","state":"Oregon","county":"Marion County","otherGeospatial":"Mill Creek, Willamette Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -123.0,44.75 ], [ -123.0,45.0 ], [ -122.875,45.0 ], [ -122.875,44.75 ], [ -123.0,44.75 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8694","contributors":{"authors":[{"text":"Tolan, Terry L.","contributorId":31029,"corporation":false,"usgs":true,"family":"Tolan","given":"Terry","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":205206,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Beeson, Marvin H.","contributorId":67937,"corporation":false,"usgs":true,"family":"Beeson","given":"Marvin","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":205208,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"DuRoss, Christopher B.","contributorId":64298,"corporation":false,"usgs":true,"family":"DuRoss","given":"Christopher B.","affiliations":[],"preferred":false,"id":205207,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30871,"text":"wri004197 - 2000 - Computer-model analysis of ground-water flow and simulated effects of contaminant remediation at Naval Weapons Industrial Reserve Plant, Dallas, Texas","interactions":[],"lastModifiedDate":"2017-01-12T13:15:59","indexId":"wri004197","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4197","title":"Computer-model analysis of ground-water flow and simulated effects of contaminant remediation at Naval Weapons Industrial Reserve Plant, Dallas, Texas","docAbstract":"In June 1993, the Department of the Navy, Southern Division Naval Facilities Engineering Command (SOUTHDIV), began a Resource Conservation and Recovery Act (RCRA) Facility Investigation (RFI) of the Naval Weapons Industrial Reserve Plant (NWIRP) in north-central Texas. The RFI has found trichloroethene, dichloroethene, vinyl chloride, as well as chromium, lead, and other metallic residuum in the shallow alluvial aquifer underlying NWIRP.
These findings and the possibility of on-site or off-site migration of contaminants prompted the need for a ground-water-flow model of the NWIRP area. The resulting U.S. Geological Survey (USGS) model: (1) defines aquifer properties, (2) computes water budgets, (3) delineates major flowpaths, and (4) simulates hydrologic effects of remediation activity. In addition to assisting with particle-tracking analyses, the calibrated model could support solute-transport modeling as well as help evaluate the effects of potential corrective action. The USGS model simulates steadystate and transient conditions of ground-water flow within a single model layer.
The alluvial aquifer is within fluvial terrace deposits of Pleistocene age, which unconformably overlie the relatively impermeable Eagle Ford Shale of Late Cretaceous age. Over small distances and short periods, finer grained parts of the aquifer are separated hydraulically; however, most of the aquifer is connected circuitously through randomly distributed coarser grained sediments. The top of the underlying Eagle Ford Shale, a regional confining unit, is assumed to be the effective lower limit of ground-water circulation and chemical contamination.
The calibrated steady-state model reproduces long-term average water levels within +5.1 or –3.5 feet of those observed; the standard error of the estimate is 1.07 feet with a mean residual of 0.02 foot. Hydraulic conductivity values range from 0.75 to 7.5 feet per day, and average about 4 feet per day. Specific yield values range from 0.005 to 0.15 and average about 0.08. Simulated infiltration rates range from 0 to 2.5 inches per year, depending mostly on local patterns of ground cover.
Computer simulation indicates that, as of December 31, 1998, remediation systems at NWIRP were removing 7,375 cubic feet of water per day from the alluvial aquifer, with 3,050 cubic feet per day coming from aquifer storage. The resulting drawdown prevented 1,800 cubic feet per day of ground water from discharging into Cottonwood Bay, as well as inducing another 1,325 cubic feet per day into the aquifer from the bay. An additional 1,200 cubic feet of water per day (compared to pre-remediation conditions) was prevented from discharging into the west lagoon, east lagoon, Mountain Creek Lake, and Mountain Creek swale.
Particle-tracking simulations, assuming an aquifer porosity of 0.15, were made to delineate flowpath patterns, or contaminant “capture zones,” resulting from 2.5- and 5-year periods of remediation activity at NWIRP. The resulting flowlines indicate three such zones, or areas from which ground water is simulated to have been removed during July 1996–December 1998, as well as extended areas from which ground water would be removed during the next 2.5 years (January 1999– June 2001).
Simulation indicates that, as of December 31, 1998, the recovery trench was intercepting about 827 cubic feet per day of ground water that—without the trench—would have discharged into Cottonwood Bay. During this time, the trench is simulated to have removed about 3,221 cubic feet per day of water from the aquifer, with about 934 cubic feet per day (29 percent) coming from the south (Cottonwood Bay) side of the trench.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004197","collaboration":"In cooperation with the Department of the Navy, Southern Division Naval Facilities Engineering Command","usgsCitation":"Barker, R.A., and Braun, C.L., 2000, Computer-model analysis of ground-water flow and simulated effects of contaminant remediation at Naval Weapons Industrial Reserve Plant, Dallas, Texas: U.S. Geological Survey Water-Resources Investigations Report 2000-4197, HTML Document; Report: v, 44 p.; 2 Plates: 36.5 x 28 inches and 18 x 18.5 inches, https://doi.org/10.3133/wri004197.","productDescription":"HTML Document; Report: v, 44 p.; 2 Plates: 36.5 x 28 inches and 18 x 18.5 inches","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":161442,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri004197.JPG"},{"id":2782,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri004197/","linkFileType":{"id":5,"text":"html"}},{"id":333097,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/wri004197/pdf/00-4197.pdf","text":"Report","size":"2.57 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":333098,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004197/pdf/pl2.pdf","text":"Plate 2","size":"617 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":333099,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004197/pdf/pl1.pdf","text":"Plate 1","size":"578 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"Texas","city":"Dallas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.73187255859375,\n 32.560703522325156\n ],\n [\n -96.9873046875,\n 32.56764789050999\n ],\n [\n -97.5,\n 32.6\n ],\n [\n -97.53387451171875,\n 32.80112754111693\n ],\n [\n -97.470703125,\n 32.99484290420988\n ],\n [\n -96.86920166015625,\n 33.23639027157906\n ],\n [\n -96.59454345703125,\n 33.24098472320831\n ],\n [\n -96.5,\n 33\n ],\n [\n -96.52313232421875,\n 32.62087018318113\n ],\n [\n -96.73187255859375,\n 32.560703522325156\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b19e4b07f02db6a75be","contributors":{"authors":[{"text":"Barker, Rene A.","contributorId":82669,"corporation":false,"usgs":true,"family":"Barker","given":"Rene","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":204246,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Braun, Christopher L. 0000-0002-5540-2854 clbraun@usgs.gov","orcid":"https://orcid.org/0000-0002-5540-2854","contributorId":925,"corporation":false,"usgs":true,"family":"Braun","given":"Christopher","email":"clbraun@usgs.gov","middleInitial":"L.","affiliations":[{"id":48595,"text":"Oklahoma-Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":204245,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":30868,"text":"wri004152 - 2000 - Geology, hydrology, and ground-water quality of the Galena-Platteville aquifer in the vicinity of the Parson's Casket Hardware Superfund Site, Belvidere, Illinois","interactions":[],"lastModifiedDate":"2024-05-29T20:47:44.065881","indexId":"wri004152","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4152","displayTitle":"Geology, Hydrology, and Ground-Water Quality of the Galena-Platteville Aquifer in the Vicinity of the Parson’s Casket Hardware Superfund Site, Belvidere, Illinois","title":"Geology, hydrology, and ground-water quality of the Galena-Platteville aquifer in the vicinity of the Parson's Casket Hardware Superfund Site, Belvidere, Illinois","docAbstract":"The geology, hydrology, and distribution of contaminants in the Galena-Platteville aquifer in the vicinity of the Parson's Casket Hardware Superfund site in northeastern Belvidere, Ill., were characterized on the basis of data collected from boreholes using geophysical logging and packer assemblies. Horizontal flow in the Galena-Platteville aquifer is affected by a network of subhorizontal fractures that are concentrated in the weathered part of the bedrock, vugs and fractures present from the bottom of the weathered bedrock to the top of a shaley layer at about 662 ft (feet) above sea level, and through a widespread subhorizontal fracture at about 524 ft. Inclined fractures provide pathways for vertical flow within the Galena-Platteville aquifer. Some fractures and flow pathways appear to be affected by the stratigraphy of the Galena-Platteville deposits.
Water-level data indicate the potential for downward flow within the Galena-Platteville aquifer. During periods when pumping in nearby municipal-supply wells is minimal or absent, the direction of flow through the fracture at about 524 ft above sea level is south toward two industrial-supply wells. Flow through the fracture is toward the municipal-supply wells when they are being pumped. Flow in the upper part of the Galena-Platteville aquifer does not appear to be affected by pumping in nearby water-supply wells.
Chlorinated ethenes were the volatile organic compounds detected most often and at the highest concentration in the Galena-Platteville aquifer beneath northeastern Belvidere. Volatile organic compounds are migrating primarily to the southeast toward the Kishwaukee River, with components of movement to the north, east, and west. Volatile organic compound and monitored natural attenuation parameter data indicate reductive dechlorination of some chlorinated ethene compounds is occurring under either nitrate or iron-reducing conditions in the unconsolidated deposits and possibly the upper part of the Galena-Platteville aquifer near the center of the plume. Oxidizing conditions appear to be present at least in the upper part of the aquifer beneath most of the study area, and the occurrence of reductive dechlorination in the Galena-Platteville aquifer beneath most of the area of investigation is not clearly indicated.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004152","collaboration":"Prepared in cooperation with the Illinois Environmental Protection Agency","usgsCitation":"Kay, R.T., 2000, Geology, hydrology, and ground-water quality of the Galena-Platteville aquifer in the vicinity of the Parson's Casket Hardware Superfund Site, Belvidere, Illinois: U.S. Geological Survey Water-Resources Investigations Report 2000-4152, v., 34 p., https://doi.org/10.3133/wri004152.","productDescription":"v., 34 p.","costCenters":[{"id":344,"text":"Illinois Water Science Center","active":true,"usgs":true}],"links":[{"id":429367,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_37088.htm","linkFileType":{"id":5,"text":"html"}},{"id":2779,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4152/wrir00_4152.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 00–4152"},{"id":161375,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4152/coverthb.jpg"}],"country":"United States","state":"Illinois","city":"Belvidere","otherGeospatial":"Parson's Casket Hardware Superfund site","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -88.83942963287024,\n 42.27140090664139\n ],\n [\n -88.83942963287024,\n 42.264209787102345\n ],\n [\n -88.82460978475213,\n 42.264209787102345\n ],\n [\n -88.82460978475213,\n 42.27140090664139\n ],\n [\n -88.83942963287024,\n 42.27140090664139\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","contact":"Director, Central Midwest Water Science Center
U.S. Geological Survey
405 North Goodwin
Urbana, IL 61801
A shallow alluvial aquifer at the Naval Weapons Industrial Reserve Plant near Dallas, Texas, has been contaminated by organic solvents used in the fabrication and assembly of aircraft and aircraft parts. Natural gamma-ray and electromagnetic-induction log data collected during 1997 from 162 wells were integrated with existing lithologic and cone-penetrometer test log data to improve characterization of the subsurface alluvium at the site. The alluvium, consisting of mostly fine-grained, low-permeability sediments, was classified into low, intermediate, and high clay-content sediments on the basis of the gamma-ray logs. Low clay-content sediments were interpreted as being relatively permeable, whereas high clay-content sediments were interpreted as being relatively impermeable. Gamma-ray logs, cone-penetrometer test logs, and electromagnetic-induction logs were used to develop a series of intersecting sections to delineate the spatial distribution of low, intermediate, and high clay-content sediments and to delineate zones of potentially contaminated sediments.
The sections indicate three major sedimentary units in the shallow alluvial aquifer at NWIRP. The lower unit consists of relatively permeable, low clay-content sediments and is absent over the southeastern and northwestern part of the site. Permeable zones in the complex, discontinuous middle unit are present mostly in the western part of the site. In the eastern and southeastern part of the site, the upper unit has been eroded away and replaced by fill material. Zones of potentially contaminated sediments are generally within the uppermost clay layer or fill material. In addition, the zones tend to be local occurrences.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri20004150","collaboration":"Prepared in cooperation with the Southern Division Naval Facilities Engineering Command","usgsCitation":"Anaya, R., Braun, C.L., and Kuniansky, E.L., 2000, Use of borehole geophysical logs for improved site characterization at Naval Weapons Industrial Reserve Plant, Dallas, Texas: U.S. Geological Survey Water-Resources Investigations Report 2000-4150, HTNL Document; Report: iv, 10 p.; 3 Plates: 36 x 20.5 inches or less, https://doi.org/10.3133/wri20004150.","productDescription":"HTNL Document; Report: iv, 10 p.; 3 Plates: 36 x 20.5 inches or less","additionalOnlineFiles":"Y","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true},{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":158452,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri20004150.JPG"},{"id":12062,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wri004150/","linkFileType":{"id":5,"text":"html"}},{"id":333144,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/wri004150/pdf/00-4150.pdf","text":"Report","size":"533 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":333145,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004150/pdf/pl2.pdf","text":"Plate 2","size":"534 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":333146,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004150/pdf/pl3.pdf","text":"Plate 3","size":"661 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 3"},{"id":333143,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004150/pdf/pl1.pdf","text":"Plate 1","size":"348 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"Texas","city":"Dallas","otherGeospatial":"Naval Weapons Industrial Reserve Plant","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -97,32.71666666666667 ], [ -97,32.75 ], [ -96.96666666666667,32.75 ], [ -96.96666666666667,32.71666666666667 ], [ -97,32.71666666666667 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6858e2","contributors":{"authors":[{"text":"Anaya, Roberto","contributorId":10827,"corporation":false,"usgs":true,"family":"Anaya","given":"Roberto","email":"","affiliations":[],"preferred":false,"id":195463,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Braun, Christopher L. 0000-0002-5540-2854 clbraun@usgs.gov","orcid":"https://orcid.org/0000-0002-5540-2854","contributorId":925,"corporation":false,"usgs":true,"family":"Braun","given":"Christopher","email":"clbraun@usgs.gov","middleInitial":"L.","affiliations":[{"id":48595,"text":"Oklahoma-Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195461,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kuniansky, Eve L. 0000-0002-5581-0225 elkunian@usgs.gov","orcid":"https://orcid.org/0000-0002-5581-0225","contributorId":932,"corporation":false,"usgs":true,"family":"Kuniansky","given":"Eve","email":"elkunian@usgs.gov","middleInitial":"L.","affiliations":[{"id":509,"text":"Office of the Associate Director for Water","active":true,"usgs":true},{"id":5064,"text":"Southeast Regional Director's Office","active":true,"usgs":true}],"preferred":true,"id":195462,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":29329,"text":"wri20004102 - 2000 - Suspended sediment in the Indiana Harbor Canal and the Grand Calumet River, northwestern Indiana, May 1996-June 1998","interactions":[],"lastModifiedDate":"2022-12-16T19:38:06.047806","indexId":"wri20004102","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4102","title":"Suspended sediment in the Indiana Harbor Canal and the Grand Calumet River, northwestern Indiana, May 1996-June 1998","docAbstract":"Suspended-sediment samples and streamflow data were collected from May 1996 through June 1998 at three sites in the Grand Calumet River Basin - Indiana Harbor Canal at East Chicago, the east branch of the Grand Calumet River at Gary, and the west branch of the Grand Calumet River at Hammond. Sample analysis allowed for retention of sediments of 0.0015 millimeters or larger.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Indianapolis, IN","doi":"10.3133/wri20004102","collaboration":"Prepared in cooperation with the US Army Corps of Engineers","usgsCitation":"Renn, D.E., 2000, Suspended sediment in the Indiana Harbor Canal and the Grand Calumet River, northwestern Indiana, May 1996-June 1998: U.S. Geological Survey Water-Resources Investigations Report 2000-4102, v, 52 p., https://doi.org/10.3133/wri20004102.","productDescription":"v, 52 p.","startPage":"1","onlineOnly":"N","additionalOnlineFiles":"N","temporalStart":"1996-05-01","temporalEnd":"1998-06-30","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":159219,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":410642,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34801.htm","linkFileType":{"id":5,"text":"html"}},{"id":12874,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/2000/wri00-4102/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Indiana","otherGeospatial":"Indiana Harbor Canal, Grand Calumet River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.563,\n 41.583\n ],\n [\n -87.563,\n 41.6667\n ],\n [\n -87.25,\n 41.6667\n ],\n [\n -87.25,\n 41.583\n ],\n [\n -87.563,\n 41.583\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fae49","contributors":{"authors":[{"text":"Renn, Danny E.","contributorId":14808,"corporation":false,"usgs":true,"family":"Renn","given":"Danny","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":201355,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":29355,"text":"wri004135 - 2000 - Methods for estimating low-flow statistics for Massachusetts streams","interactions":[],"lastModifiedDate":"2012-02-02T00:08:49","indexId":"wri004135","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4135","title":"Methods for estimating low-flow statistics for Massachusetts streams","docAbstract":"Methods and computer software are described in this report for determining flow duration, low-flow frequency statistics, and August median flows. These low-flow statistics can be estimated for unregulated streams in Massachusetts using different methods depending on whether the location of interest is at a streamgaging station, a low-flow partial-record station, or an ungaged site where no data are available. Low-flow statistics for streamgaging stations can be estimated using standard U.S. Geological Survey methods described in the report. The MOVE.1 mathematical method and a graphical correlation method can be used to estimate low-flow statistics for low-flow partial-record stations. The MOVE.1 method is recommended when the relation between measured flows at a partial-record station and daily mean flows at a nearby, hydrologically similar streamgaging station is linear, and the graphical method is recommended when the relation is curved. Equations are presented for computing the variance and equivalent years of record for estimates of low-flow statistics for low-flow partial-record stations when either a single or multiple index stations are used to determine the estimates. The drainage-area ratio method or regression equations can be used to estimate low-flow statistics for ungaged sites where no data are available. The drainage-area ratio method is generally as accurate as or more accurate than regression estimates when the drainage-area ratio for an ungaged site is between 0.3 and 1.5 times the drainage area of the index data-collection site. Regression equations were developed to estimate the natural, long-term 99-, 98-, 95-, 90-, 85-, 80-, 75-, 70-, 60-, and 50-percent duration flows; the 7-day, 2-year and the 7-day, 10-year low flows; and the August median flow for ungaged sites in Massachusetts. Streamflow statistics and basin characteristics for 87 to 133 streamgaging stations and low-flow partial-record stations were used to develop the equations. The streamgaging stations had from 2 to 81 years of record, with a mean record length of 37 years. The low-flow partial-record stations had from 8 to 36 streamflow measurements, with a median of 14 measurements. All basin characteristics were determined from digital map data. The basin characteristics that were statistically significant in most of the final regression equations were drainage area, the area of stratified-drift deposits per unit of stream length plus 0.1, mean basin slope, and an indicator variable that was 0 in the eastern region and 1 in the western region of Massachusetts. The equations were developed by use of weighted-least-squares regression analyses, with weights assigned proportional to the years of record and inversely proportional to the variances of the streamflow statistics for the stations. Standard errors of prediction ranged from 70.7 to 17.5 percent for the equations to predict the 7-day, 10-year low flow and 50-percent duration flow, respectively. The equations are not applicable for use in the Southeast Coastal region of the State, or where basin characteristics for the selected ungaged site are outside the ranges of those for the stations used in the regression analyses. A World Wide Web application was developed that provides streamflow statistics for data collection stations from a data base and for ungaged sites by measuring the necessary basin characteristics for the site and solving the regression equations. Output provided by the Web application for ungaged sites includes a map of the drainage-basin boundary determined for the site, the measured basin characteristics, the estimated streamflow statistics, and 90-percent prediction intervals for the estimates. An equation is provided for combining regression and correlation estimates to obtain improved estimates of the streamflow statistics for low-flow partial-record stations. An equation is also provided for combining regression and drainage-area ratio estimates to obtain improved e","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri004135","usgsCitation":"Ries, K., and Friesz, P.J., 2000, Methods for estimating low-flow statistics for Massachusetts streams: U.S. Geological Survey Water-Resources Investigations Report 2000-4135, v, 81 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri004135.","productDescription":"v, 81 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":2295,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004135","linkFileType":{"id":5,"text":"html"}},{"id":159425,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62a1ab","contributors":{"authors":[{"text":"Ries, Kernell G. III kries@usgs.gov","contributorId":1913,"corporation":false,"usgs":true,"family":"Ries","given":"Kernell G.","suffix":"III","email":"kries@usgs.gov","affiliations":[{"id":502,"text":"Office of Surface Water","active":true,"usgs":true}],"preferred":false,"id":201398,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Friesz, Paul J. 0000-0002-4660-2336 pfriesz@usgs.gov","orcid":"https://orcid.org/0000-0002-4660-2336","contributorId":1075,"corporation":false,"usgs":true,"family":"Friesz","given":"Paul","email":"pfriesz@usgs.gov","middleInitial":"J.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":201397,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":31170,"text":"ofr00356 - 2000 - Geologic map of the Wildcat Lake 7.5' quadrangle, Kitsap and Mason Counties, Washington","interactions":[],"lastModifiedDate":"2023-11-06T15:31:21.339206","indexId":"ofr00356","displayToPublicDate":"2001-07-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2000-356","title":"Geologic map of the Wildcat Lake 7.5' quadrangle, Kitsap and Mason Counties, Washington","docAbstract":"The Wildcat Lake quadrangle lies in the forearc of the Cascadia subduction zone, about 20-km east of the Cascadia accretionary complex exposed in the Olympic Mountains (Tabor and Cady, 1978),and about 100-km west of the axis of the Cascades volcanic arc. The quadrangle lies near the middle of the Puget Lowland, which typically has elevations less than 600 feet (183 m), but on Gold Mountain, in the center of the quadrangle, the elevation rises to 1761 feet (537 m). This anomalously high topography also provides a glimpse of the deeper crust beneath the Lowland. Exposed on Green and Gold Mountains are rocks related to the Coast Range basalt terrane. This terrane consists of Eocene submarine and subaerial tholeiitic basalt of the Crescent Formation, which probably accreted to the continental margin in Eocene time (Snavely and others, 1968). The Coast Range basalt terrane may have originated as an oceanic plateau or by oblique marginal rifting (Babcock and others, 1992), but its subsequent emplacement history is complex (Wells and others, 1984). In southern Oregon, onlapping strata constrain the suturing to have occurred by 50 Ma; but on southern Vancouver Island where the terrane-bounding Leech River fault is exposed, Brandon and Vance (1992) concluded suturing to North America occurred in the broad interval between 42 and 24 Ma. After emplacement of the Coast Range basalt terrane, the Cascadia accretionary complex,exposed in the Olympic Mountains west of the quadrangle,developed by frontal accretion and underplating (e.g., Clowes and others, 1987). The Seattle basin, part of which lies to the north of Green Mountain, also began to develop in late Eocene time due to forced flexural subsidence along the Seattle fault zone (Johnson and others, 1994). Domal uplift of the accretionary complex beneath the Olympic Mountains occurred after approximately 18 million years ago (Brandon and others, 1998). Ice-sheet glaciation during Quaternary time reshaped the topography of the quadrangle, and approximately two-thirds of the map area is covered with Quaternary deposits related to the last glaciation. Geophysical studies and regional mapping indicate the Seattle fault lies north of Green Mountain. This fault produced a large earthquake about 1000 years ago and may pose a significant earthquake hazard (Bucknam and others, 1992; Atwater and Moore, 1992; Karlin and Abella,1992; Schuster and others, 1992; Jacoby and others, 1992). We found no evidence of Holocene faulting in the Wildcat Lake quadrangle.
Geologic mapping within and marginal to the quadrangle began with Willis (1898), who described glacial deposits in Puget Sound. Weaver (1937) correlated volcanic rocks in the quadrangle to the Eocene Metchosin Volcanics on Vancouver Island. Sceva (1957), Garling and Moleenar (1965), and Deeter (1978) all focused on mapping and understanding the Quaternary stratigraphy of the Kitsap Peninsula, but they also examined bedrock in the quadrangle. Reeve (1979) was the first to examine the igneous rocks on Green and Gold Mountains in some detail, and Clark (1989) significantly improved Reeve's (1979) mapping. Clark's (1989) mapping was conducted soon after extensive logging on the mountains. A surficial geologic map of the Seattle 1:100,000-scale quadrangle, which includes the Wildcat Lake 1:24,000-scale quadrangle, was published by Yount and others (1993). Yount and Gower (1991) also published a bedrock geologic map of the Seattle quadrangle. Geologic mapping for this report was conducted by Haeussler in the spring and summer of 1998 and in the winter of 1999. We could not substantially improve upon the bedrock mapping of Clark (1989) and thus it is incorporated into this map. Well data in the southeastern corner of the map area also helped to constrain the surficial mapping (Geomatrix Consultants, 1997). In addition, 1995 vintage 1:12,000-scale aerial photographs were used in mapping Quaternary deposits. Geologic time scale is that of Berggeren and others (1995).
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr00356","usgsCitation":"Haeussler, P.J., and Clark, K.P., 2000, Geologic map of the Wildcat Lake 7.5' quadrangle, Kitsap and Mason Counties, Washington: U.S. Geological Survey Open-File Report 2000-356, Report: 14 p.; 1 Plate: 37.89 x 34.67 inches; Metadata, https://doi.org/10.3133/ofr00356.","productDescription":"Report: 14 p.; 1 Plate: 37.89 x 34.67 inches; Metadata","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":125447,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2000_356.jpg"},{"id":391428,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34290.htm"},{"id":2677,"rank":5,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/0356/","linkFileType":{"id":5,"text":"html"}},{"id":281618,"rank":2,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2000/0356/of00-356.ps"},{"id":281617,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/2000/0356/pdf/of00-356.pdf"}],"scale":"24000","projection":"Universal Transverse Mercator projection","datum":"1927 North American datum","country":"United States","state":"Washington","county":"Kitsap County, Mason County","otherGeospatial":"Gold Mountain, Olympic Mountains, Wildcat Lake quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122.875,47.5 ], [ -122.875,47.625 ], [ -122.75,47.625 ], [ -122.75,47.5 ], [ -122.875,47.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4823e4b07f02db4e25ae","contributors":{"authors":[{"text":"Haeussler, Peter J. 0000-0002-1503-6247 pheuslr@usgs.gov","orcid":"https://orcid.org/0000-0002-1503-6247","contributorId":503,"corporation":false,"usgs":true,"family":"Haeussler","given":"Peter","email":"pheuslr@usgs.gov","middleInitial":"J.","affiliations":[{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":205209,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Clark, Kenneth P.","contributorId":65513,"corporation":false,"usgs":true,"family":"Clark","given":"Kenneth","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":205210,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":27166,"text":"wri004110 - 2000 - Estimating the probability of elevated nitrate (NO2+NO3-N) concentrations in ground water in the Columbia Basin Ground Water Management Area, Washington","interactions":[],"lastModifiedDate":"2023-01-11T19:33:39.924408","indexId":"wri004110","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4110","displayTitle":"Estimating the probability of elevated nitrate (NO2+NO3-N) concentrations in ground water in the Columbia Basin Ground Water Management Area, Washington","title":"Estimating the probability of elevated nitrate (NO2+NO3-N) concentrations in ground water in the Columbia Basin Ground Water Management Area, Washington","docAbstract":"Logistic regression was used to relate anthropogenic (man-made) and natural factors to the occurrence of elevated concentrations of nitrite plus nitrate as nitrogen in ground water in the Columbia Basin Ground Water Management Area, eastern Washington. Variables that were analyzed included well depth, depth of well casing, ground-water recharge rates, presence of canals, fertilizer application amounts, soils, surficial geology, and land-use types. The variables that best explain the occurrence of nitrate concentrations above 3 milligrams per liter in wells were the amount of fertilizer applied annually within a 2-kilometer radius of a well and the depth of the well casing; the variables that best explain the occurrence of nitrate above 10 milligrams per liter included the amount of fertilizer applied annually within a 3-kilometer radius of a well, the depth of the well casing, and the mean soil hydrologic group, which is a measure of soil infiltration rate. Based on the relations between these variables and elevated nitrate concentrations, models were developed using logistic regression that predict the probability that ground water will exceed a nitrate concentration of either 3 milligrams per liter or 10 milligrams per liter. Maps were produced that illustrate the predicted probability that ground-water nitrate concentrations will exceed 3 milligrams per liter or 10 milligrams per liter for wells cased to 78 feet below land surface (median casing depth) and the predicted depth to which wells would need to be cased in order to have an 80-percent probability of drawing water with a nitrate concentration below either 3 milligrams per liter or 10 milligrams per liter. Maps showing the predicted probability for the occurrence of elevated nitrate concentrations indicate that the irrigated agricultural regions are most at risk. The predicted depths to which wells need to be cased in order to have an 80-percent chance of obtaining low nitrate ground water exceed 600 feet in the irrigated agricultural regions, whereas wells in dryland agricultural areas generally need a casing in excess of 400 feet. The predicted depth to which wells need to be cased to have at least an 80-percent chance to draw water with a nitrate concentration less than 10 milligrams per liter generally did not exceed 800 feet, with a 200-foot casing depth typical of the majority of the area.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004110","usgsCitation":"Frans, L.M., 2000, Estimating the probability of elevated nitrate (NO2+NO3-N) concentrations in ground water in the Columbia Basin Ground Water Management Area, Washington: U.S. Geological Survey Water-Resources Investigations Report 2000-4110, iv, 26 p., https://doi.org/10.3133/wri004110.","productDescription":"iv, 26 p.","costCenters":[],"links":[{"id":158021,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":411729,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_33855.htm","linkFileType":{"id":5,"text":"html"}},{"id":2128,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004110/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Washington","otherGeospatial":"Columbia Basin Ground Water Management Area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118,\n 48\n ],\n [\n -120,\n 48\n ],\n [\n -120,\n 46.26\n ],\n [\n -118,\n 46.26\n ],\n [\n -118,\n 48\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ae4b07f02db5fb984","contributors":{"authors":[{"text":"Frans, Lonna M. 0000-0002-3217-1862 lmfrans@usgs.gov","orcid":"https://orcid.org/0000-0002-3217-1862","contributorId":1493,"corporation":false,"usgs":true,"family":"Frans","given":"Lonna","email":"lmfrans@usgs.gov","middleInitial":"M.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"preferred":true,"id":197673,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28209,"text":"wri004148 - 2000 - Hydrogeology, hydrologic budget, and water chemistry of the Medina Lake area, Texas","interactions":[],"lastModifiedDate":"2017-03-29T17:28:32","indexId":"wri004148","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4148","title":"Hydrogeology, hydrologic budget, and water chemistry of the Medina Lake area, Texas","docAbstract":"A three-phase study of the Medina Lake area in Texas was done to assess the hydrogeology and hydrology of Medina and Diversion Lakes combined (the lake system) and to determine what fraction of seepage losses from the lake system might enter the regional ground-water-flow system of the Edwards and (or) Trinity aquifers. Phase 1 consisted of revising the geologic framework for the Medina Lake area. Results of field mapping show that the upper member of the Glen Rose Limestone underlies Medina Lake and the intervening stream channel from the outflow of Medina Lake to the midpoint of Diversion Lake, where the Diversion Lake fault intersects Diversion Lake. A thin sequence of strata consisting primarily of the basal nodular and dolomitic members of the Kainer Formation of the Edwards Group, is present in the southern part of the study area. On the southern side of Medina Lake, the contact between the upper member of the Glen Rose Limestone and the basal nodular member is approximately 1,000 feet above mean sea level, and the contact between the basal nodular member and the dolomitic member is approximately 1,050 feet above mean sea level. The most porous and permeable part of the basal nodular member is about 1,045 feet above mean sea level. At these altitudes, Medina Lake is in hydrologic connection with rocks in the Edwards aquifer recharge zone, and Medina Lake appears to lose more water to the ground-water system along this bedding plane contact.
Hydrologic budgets calculated during phase 2 for Medina Lake, Diversion Lake, and Medina/Diversion Lakes combined indicate that: (1) losses from Medina and Diversion Lakes can be quantified; (2) a portion of those losses are entering the Edwards aquifer; and (3) losses to the Trinity aquifer in the Medina Lake area are minimal and within the error of the hydrologic budgets.
Hydrologic budgets based on streamflow, precipitation, evaporation, and change in lake storage were used to quantify losses (recharge) to the ground-water system from Medina Lake, Diversion Lake, and Medina/Diversion Lakes combined during October 1995–September 1996. Water losses from Medina Lake to the Edwards/Trinity aquifers ranged from -14.0 to 135 acre-feet per day; Diversion Lake ranged from -1.2 to 93.1 acre-feet per day; and Medina/Diversion Lakes combined ranged from 36.1 to 119 acre-feet per day.
Monthly average recharge during December 1995–July 1996 was estimated using an alternative method developed during this study (current study method) and compared to monthly average recharge during December 1995–July 1996 estimated using the existing USGS method and the Trans-Texas method. Recharge to the Edwards aquifer estimated using the current study method was about 69 and 73 percent of the recharge estimated using the USGS and Trans-Texas methods, respectively. The USGS and Trans-Texas methods overestimated recharge from Medina Lake compared to the recharge estimated with the current study method when Medina Lake stage was between about 1,027 and 1,032 feet above mean sea level and underestimated recharge from Medina Lake when lake stage was between about 1,036 and 1,045 feet above mean sea level. The USGS and Trans-Texas methods underestimated recharge from Diversion Lake compared to the recharge estimated with the current study method when Diversion Lake stage was greater than 913 feet above mean sea level and overestimated recharge from Diversion Lake when lake stage was less than 913 feet above mean sea level.
The water quality of Medina Lake and Medina River and in selected wells and springs in the Edwards and Trinity aquifers was characterized during phase 3 of the study. Environmental isotope analyses and geochemical modeling also were used to determine where water losses from the lake system might be entering the ground-water-flow system. Isotopic ratios of deuterium, oxygen, and strontium were analyzed in selected surface-water, lake-water, and ground-water samples to trace the isotopic “signature” of the lake water as it mixes with the ground water and to determine the fraction of lake water and ground water in selected Edwards aquifer wells. Isotopic data and geochemical modeling were used to show that lake water is moving into the Edwards aquifer in two fault blocks in the eastern Medina storage unit. One fault block is bounded on the north by the Vandenburg School fault and on the south by the Haby Crossing fault, and the second fault block is bounded on the north by the Diversion Lake fault and on the south by the Haby Crossing fault. In selected Edwards aquifer wells located southwest of Medina Lake and west of Diversion Lake, the proportion of lake water ranged from about 10 to 45 percent. Geochemical modeling using NETPATH confirms the degree of mixing between lake water and aquifer water shown by the isotopes.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004148","collaboration":"In cooperation with the Bexar-Medina-Atascosa Counties Water Control and Improvement District No. 1, Bexar Metropolitan Water District, Texas Water Development Board, and Edwards Aquifer Authority","usgsCitation":"Lambert, R.B., Grimm, K.C., and Lee, R.W., 2000, Hydrogeology, hydrologic budget, and water chemistry of the Medina Lake area, Texas: U.S. Geological Survey Water-Resources Investigations Report 2000-4148, Report: v, 54 p.; 2 Plates: 30.00 x 25.00 inches and 25.00 x 25.50 inches, https://doi.org/10.3133/wri004148.","productDescription":"Report: v, 54 p.; 2 Plates: 30.00 x 25.00 inches and 25.00 x 25.50 inches","numberOfPages":"190","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":159580,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri004148.PNG"},{"id":328031,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/wri004148/pdf/wri00-4148.pdf","text":"Report","size":"9.16 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":328032,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004148/pdf/00-4148_pl1.pdf","text":"Plate 1","size":"1.11 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"},{"id":328033,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/wri004148/pdf/00-4148_pl2.pdf","text":"Plate 2","size":"1.57 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":2328,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004148/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Texas","otherGeospatial":"Medina Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -99.05479431152344,\n 29.432421529604852\n ],\n [\n -98.84536743164061,\n 29.432421529604852\n ],\n [\n -98.84536743164061,\n 29.7375511168952\n ],\n [\n -99.05479431152344,\n 29.7375511168952\n ],\n [\n -99.05479431152344,\n 29.432421529604852\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8639","contributors":{"authors":[{"text":"Lambert, Rebecca B. 0000-0002-0611-1591 blambert@usgs.gov","orcid":"https://orcid.org/0000-0002-0611-1591","contributorId":1135,"corporation":false,"usgs":true,"family":"Lambert","given":"Rebecca","email":"blambert@usgs.gov","middleInitial":"B.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":199398,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Grimm, Kenneth C.","contributorId":29483,"corporation":false,"usgs":true,"family":"Grimm","given":"Kenneth","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":199399,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lee, Roger W.","contributorId":105273,"corporation":false,"usgs":true,"family":"Lee","given":"Roger","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":199400,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":26043,"text":"wri004093 - 2000 - Two months of flooding in eastern North Carolina, September-October 1999: Hydrologic, water-quality, and geologic effects of hurricanes Dennis, Floyd, and Irene","interactions":[],"lastModifiedDate":"2021-11-05T20:53:01.008314","indexId":"wri004093","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4093","title":"Two months of flooding in eastern North Carolina, September-October 1999: Hydrologic, water-quality, and geologic effects of hurricanes Dennis, Floyd, and Irene","docAbstract":"The combined effects of Hurricanes Dennis, Floyd, and Irene in September and October 1999 resulted in 2 months of flooding throughout most of eastern North Carolina. Hurricane Dennis battered the Outer Banks for almost a week in early September, resulting in severe shore- line erosion in some locations near Buxton and Rodanthe. Upon making landfall less than 2 weeks before Hurricane Floyd, Hurricane Dennis delivered 4 to 8 inches of rain to much of the Tar and Neuse River Basins, breaking a drought and saturating soils. Hurricane Floyd will likely be the second or third most costly hurricane to strike the United States in the 20th century, resulting in more fatalities than any hurricane to strike the United States since 1972. Rainfall amounts recorded during Hurricane Floyd (September 14-17, 1999) and accumulated during the months of September and October were unprecedented for many parts of eastern North Carolina during more than 80 years of precipitation records. Most recording stations in eastern North Carolina received at least half the average annual rainfall during the 2 months. Flooding was at record levels, and 500-year or greater floods occurred in all of the State's river basins east of Raleigh. More than half of the average annual nitrogen and phosphorus loads were transported in the Neuse and Tar Rivers by floodwaters during the 1-month period between mid-September and mid-October. Shoreline erosion from the passage of Hurricane Floyd was particularly severe along Oak and Topsail Islands; the effects of Hurricane Floyd on shoreline erosion and dune retreat were greater than the effects of Hurricane Bonnie in 1998. Fortunately, Hurricane Irene in mid-October did not make landfall in North Carolina, but rainfall from the storm did help ensure that several rivers in eastern North Carolina remained above flood stage for almost 2 months.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004093","usgsCitation":"Bales, J.D., Oblinger, C.J., and Sallenger, 2000, Two months of flooding in eastern North Carolina, September-October 1999: Hydrologic, water-quality, and geologic effects of hurricanes Dennis, Floyd, and Irene: U.S. Geological Survey Water-Resources Investigations Report 2000-4093, v, 47 p., https://doi.org/10.3133/wri004093.","productDescription":"v, 47 p.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":391453,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_27051.htm"},{"id":2030,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004093","linkFileType":{"id":5,"text":"html"}},{"id":54821,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4093/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":158384,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4093/report-thumb.jpg"}],"country":"United States","state":"North Carolina","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -79.89257812499999,\n 32.731840896865684\n ],\n [\n -75.498046875,\n 32.731840896865684\n ],\n [\n -75.498046875,\n 36.54494944148322\n ],\n [\n -79.89257812499999,\n 36.54494944148322\n ],\n [\n -79.89257812499999,\n 32.731840896865684\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b02e4b07f02db6989f2","contributors":{"authors":[{"text":"Bales, Jerad D. 0000-0001-8398-6984 jdbales@usgs.gov","orcid":"https://orcid.org/0000-0001-8398-6984","contributorId":683,"corporation":false,"usgs":true,"family":"Bales","given":"Jerad","email":"jdbales@usgs.gov","middleInitial":"D.","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true},{"id":5058,"text":"Office of the Chief Scientist for Water","active":true,"usgs":true}],"preferred":true,"id":195699,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Oblinger, Carolyn J. 0000-0003-2914-1643 oblinger@usgs.gov","orcid":"https://orcid.org/0000-0003-2914-1643","contributorId":13275,"corporation":false,"usgs":true,"family":"Oblinger","given":"Carolyn","email":"oblinger@usgs.gov","middleInitial":"J.","affiliations":[],"preferred":false,"id":195700,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sallenger, Jr.","contributorId":105768,"corporation":false,"usgs":true,"family":"Sallenger","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":195701,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":22521,"text":"ofr00495 - 2000 - Geologic datasets for weights of evidence analysis in northeast Washington: 1. Geologic raster data","interactions":[],"lastModifiedDate":"2023-06-22T13:28:41.577101","indexId":"ofr00495","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2000-495","title":"Geologic datasets for weights of evidence analysis in northeast Washington: 1. Geologic raster data","docAbstract":"This dataset contains the combination of geology data (geologic units, faults, folds, and dikes) from 6 1:100,000 scale digital coverages in eastern Washington (Chewelah, Colville, Omak, Oroville, Nespelem, Republic). The data was converted to an Arc grid in ArcView using the Spatial Analyst extension.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr00495","usgsCitation":"Boleneus, D.E., and Causey, J.D., 2000, Geologic datasets for weights of evidence analysis in northeast Washington: 1. Geologic raster data: U.S. Geological Survey Open-File Report 2000-495, Report: 35 p., Readme, Metadata, Digital Database, Complete Digital Package, https://doi.org/10.3133/ofr00495.","productDescription":"Report: 35 p., Readme, Metadata, Digital Database, Complete Digital Package","numberOfPages":"35","additionalOnlineFiles":"Y","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":281976,"rank":3,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr00495.jpg"},{"id":281973,"rank":2,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/of/2000/0495/of00-495.met"},{"id":281975,"rank":1,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2000/0495/newafull.tar.gz"},{"id":281974,"rank":4,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/of/2000/0495/newa.tar.gz"},{"id":281972,"rank":6,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/of/2000/0495/00readme.txt","linkFileType":{"id":2,"text":"txt"}},{"id":1300,"rank":5,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/0495/","linkFileType":{"id":5,"text":"html"}},{"id":410875,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34735.htm","linkFileType":{"id":5,"text":"html"}},{"id":52027,"rank":8,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0495/pdf/of00-495.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Washington","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -120,\n 48\n ],\n [\n -120,\n 49\n ],\n [\n -117,\n 49\n ],\n [\n -117,\n 48\n ],\n [\n -120,\n 48\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e92f","contributors":{"authors":[{"text":"Boleneus, David E.","contributorId":87167,"corporation":false,"usgs":true,"family":"Boleneus","given":"David","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":188396,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Causey, J. Douglas","contributorId":41398,"corporation":false,"usgs":true,"family":"Causey","given":"J.","email":"","middleInitial":"Douglas","affiliations":[],"preferred":false,"id":188395,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28870,"text":"wri004066 - 2000 - Evaluation of the use of reach transmissivity to quantify leakage beneath Levee 31N, Miami-Dade County, Florida","interactions":[],"lastModifiedDate":"2023-01-10T20:24:32.317717","indexId":"wri004066","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4066","title":"Evaluation of the use of reach transmissivity to quantify leakage beneath Levee 31N, Miami-Dade County, Florida","docAbstract":"A coupled ground- and surface-water model (MODBRANCH) was developed to estimate ground-water flow beneath Levee 31N in Miami-Dade County, Florida, and to simulate hydrologic conditions in the surrounding area. The study included compilation of data from monitoring stations, measurement of vertical seepage rates in wetlands, and analysis of the hydrogeologic properties of the ground-water aquifer within the study area. In addition, the MODBRANCH code was modified to calculate the exchange between surface-water channels and ground water using a relation based on the concept of reach transmissivity. The modified reach-transmissivity version of the MODBRANCH code was successfully tested on three simple problems with known analytical solutions. It was also tested and determined to function adequately on one field problem that had previously been solved using the unmodified version of the software. The modified version of MODBRANCH was judged to have performed satisfactorily, and it required about 60 percent as many iterations to reach a solution. Additionally, its input parameters are more physically-based and less dependent on model-grid spacing. A model of the Levee 31N area was developed and used with the original and modified versions of MODBRANCH, which produced similar output. The mean annual modeled ground-water heads differed by only 0.02 foot, and the mean annual canal discharge differed by less than 1.0 cubic foot per second. Seepage meters were used to quantify vertical seepage rates in the Everglades wetlands area west of Levee 31N. A comparison between results from the seepage meters and from the computer model indicated substantial differences that seemed to be a result of local variations in the hydraulic properties in the topmost part of the Biscayne aquifer. The transmissivity of the Biscayne aquifer was estimated to be 1,400,000 square feet per day in the study area. The computer model was employed to simulate seepage of ground water beneath Levee 31N. Modeled seepage rates were usually between 100 and 400 cubic feet per day per foot of levee, but extreme values ranged from about -200 to 500 cubic feet per day (positive values indicate eastward seepage beneath the levee). The modeled seepage results were used to develop an algorithm to estimate seepage based on head differential at selected monitoring stations. The algorithm was determined to adequately predict ground-water seepage.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004066","usgsCitation":"Nemeth, M.S., Wilcox, W.M., and Solo-Gabriele, H.M., 2000, Evaluation of the use of reach transmissivity to quantify leakage beneath Levee 31N, Miami-Dade County, Florida: U.S. Geological Survey Water-Resources Investigations Report 2000-4066, iv, 80 p., https://doi.org/10.3133/wri004066.","productDescription":"iv, 80 p.","costCenters":[],"links":[{"id":159637,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":411662,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34359.htm","linkFileType":{"id":5,"text":"html"}},{"id":2344,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004066","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","county":"Miami-Dade County","otherGeospatial":"Levee 31N","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -80.417,\n 25.783\n ],\n [\n -80.583,\n 25.783\n ],\n [\n -80.583,\n 25.658\n ],\n [\n -80.417,\n 25.658\n ],\n [\n -80.417,\n 25.783\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e774d","contributors":{"authors":[{"text":"Nemeth, Mark S.","contributorId":80319,"corporation":false,"usgs":true,"family":"Nemeth","given":"Mark","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":200533,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilcox, Walter M.","contributorId":41470,"corporation":false,"usgs":true,"family":"Wilcox","given":"Walter","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":200532,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Solo-Gabriele, Helena M.","contributorId":16871,"corporation":false,"usgs":true,"family":"Solo-Gabriele","given":"Helena","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":200531,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":26328,"text":"wri004104 - 2000 - Quality-assurance design applied to an assessment of agricultural pesticides in ground water from carbonate bedrock aquifers in the Great Valley of eastern Pennsylvania","interactions":[],"lastModifiedDate":"2018-02-26T16:01:11","indexId":"wri004104","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4104","title":"Quality-assurance design applied to an assessment of agricultural pesticides in ground water from carbonate bedrock aquifers in the Great Valley of eastern Pennsylvania","docAbstract":"Assessments to determine whether agricultural pesticides are present in ground water are performed by the Commonwealth of Pennsylvania under the aquifer monitoring provisions of the State Pesticides and Ground Water Strategy. Pennsylvania's Department of Agriculture conducts the monitoring and collects samples; the Department of Environmental Protection (PaDEP) Laboratory analyzes the samples to measure pesticide concentration. To evaluate the quality of the measurements of pesticide concentration for a groundwater assessment, a quality-assurance design was developed and applied to a selected assessment area in Pennsylvania. This report describes the quality-assurance design, describes how and where the design was applied, describes procedures used to collect and analyze samples and to evaluate the results, and summarizes the quality assurance results along with the assessment results.
The design was applied in an agricultural area of the Delaware River Basin in Berks, Lebanon, Lehigh, and Northampton Counties to evaluate the bias and variability in laboratory results for pesticides. The design—with random spatial and temporal components—included four data-quality objectives for bias and variability. The spatial design was primary and represented an area comprising 30 sampling cells. A quality-assurance sampling frequency of 20 percent of cells was selected to ensure a sample number of five or more for analysis. Quality-control samples included blanks, spikes, and replicates of laboratory water and spikes, replicates, and 2-lab splits of groundwater. Two analytical laboratories, the PaDEP Laboratory and a U.S. Geological Survey Laboratory, were part of the design. Bias and variability were evaluated by use of data collected from October 1997 through January 1998 for alachlor, atrazine, cyanazine, metolachlor, simazine, pendimethalin, metribuzin, and chlorpyrifos.
Results of analyses of field blanks indicate that collection, processing, transport, and laboratory analysis procedures did not contaminate the samples; there were no false-positive results. Pesticides were detected in water when pesticides were spiked into (added to) samples. There were no false negatives for the eight pesticides in all spiked samples. Negative bias was characteristic of analytical results for the eight pesticides, and bias was generally in excess of 10 percent from the ‘true’ or expected concentration (34 of 39 analyses, or 87 percent of the ground-water results) for pesticide concentrations ranging from 0.31 to 0.51 mg/L (micrograms per liter). The magnitude of the negative bias for the eight pesticides, with the exception of cyanazine, would result in reported concentrations commonly 75-80 percent of the expected concentration in the water sample. The bias for cyanazine was negative and within 10 percent of the expected concentration. A comparison of spiked pesticide-concentration recoveries in laboratory water and ground water indicated no effect of the ground-water matrix, and matrix interference was not a source of the negative bias. Results for the laboratory-water spikes submitted in triplicate showed large variability for recoveries of atrazine, cyanazine, and pendimethalin. The relative standard deviation (RSD) was used as a measure of method variability over the course of the study for laboratory waters at a concentration of 0.4 mg/L. An RSD of about 11 percent (or about ?0.05 mg/L)characterizes the method results for alachlor, chlorpyrifos, metolachlor, metribuzin, and simazine. Atrazine and pendimethalin have RSD values of about 17 and 23 percent, respectively. Cyanazine showed the largest RSD at nearly 51 percent. The pesticides with low variability in laboratory-water spikes also had low variability in ground water.
The assessment results showed that atrazinewas the most commonly detected pesticide in ground water in the assessment area. Atrazine was detected in water from 22 of the 28 wells sampled, and recovery results for atrazine were some of the worst (largest negative bias). Concentrations of the eight pesticides in ground water from wells were generally less than 0.3 µg/L. Only six individual measurements of the concentrations in water from six of the wells were at or above 0.3 µg/L, five for atrazine and one for metolachlor. There were eight additional detections of metolachlor and simazine at concentrations less than 0.1 µg/L. No well water contained more than one pesticide at concentra-tions at or above 0.3 µg/L. Evidence exists, how-ever, for a pattern of co-occurrence of metolachlor and simazine at low concentrations with higher concentrations of atrazine.
Large variability in replicate samples and negative bias for pesticide recovery from spiked samples indicate the need to use data for pesticide recovery in the interpretation of measured pesti-cide concentrations in ground water. Data from samples spiked with known amounts of pesticides were a critical component of a quality-assurance design for the monitoring component of the Pesti-cides and Ground Water Strategy.
Trigger concentrations, the concentrations that require action under the Pesticides and Ground Water Strategy, should be considered maximums for action. This consideration is needed because of the magnitude of negative bias.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri004104","collaboration":"Prepared in cooperation with the Pennsylvania Department of Agriculture","usgsCitation":"Breen, K.J., 2000, Quality-assurance design applied to an assessment of agricultural pesticides in ground water from carbonate bedrock aquifers in the Great Valley of eastern Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 2000-4104, vi, 31 p., https://doi.org/10.3133/wri004104.","productDescription":"vi, 31 p.","onlineOnly":"Y","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":2017,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4104/wri20004104.pdf","text":"Report","size":"1 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 2000-4104"},{"id":157524,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4104/coverthb.jpg"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri004114","usgsCitation":"Cecil, L.D., Knobel, L.L., Green, J.R., and Frape, S.K., 2000, In situ production of chlorine-36 in the eastern Snake River Plain aquifer, Idaho: Implications for describing ground-water contamination near a nuclear facility: U.S. Geological Survey Water-Resources Investigations Report 2000-4114, v, 35 p., https://doi.org/10.3133/wri004114.","productDescription":"v, 35 p.","costCenters":[],"links":[{"id":396267,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_33549.htm"},{"id":157579,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/2000/4114/report-thumb.jpg"},{"id":95546,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/2000/4114/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","otherGeospatial":"eastern Snake River Plain aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -113.333,\n 43.339\n ],\n [\n -111.661,\n 43.339\n ],\n [\n -111.661,\n 44.339\n ],\n [\n -113.333,\n 44.339\n ],\n [\n -113.333,\n 43.339\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fce4b07f02db5f5a47","contributors":{"authors":[{"text":"Cecil, L. DeWayne","contributorId":72828,"corporation":false,"usgs":true,"family":"Cecil","given":"L.","email":"","middleInitial":"DeWayne","affiliations":[],"preferred":false,"id":194413,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Knobel, LeRoy L.","contributorId":76285,"corporation":false,"usgs":true,"family":"Knobel","given":"LeRoy","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":194414,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Green, Jaromy R.","contributorId":57498,"corporation":false,"usgs":true,"family":"Green","given":"Jaromy","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":194411,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Frape, Shaun K.","contributorId":60681,"corporation":false,"usgs":true,"family":"Frape","given":"Shaun","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":194412,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":28699,"text":"wri004020 - 2000 - Environmental setting and its relations to water quality in the Kanawha River basin","interactions":[],"lastModifiedDate":"2012-02-02T00:08:46","indexId":"wri004020","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000-4020","title":"Environmental setting and its relations to water quality in the Kanawha River basin","docAbstract":"The Kanawha River and its major tributary, the New River, drain 12,233 mi2 in West Virginia, Virginia, and North Carolina. Altitude ranges from about 550 ft to more than 4,700 ft. The Kanawha River Basin is mountainous, and includes parts of three physiographic provinces, the Blue Ridge (17 percent), Valley and Ridge (23 percent), and Appalachian Plateaus (60 percent). In the Appalachian Plateaus Province, little of the land is flat, and most of the flat land is in the flood plains and terraces of streams; this has caused most development in this part of the basin to be near streams. The Blue Ridge Province is composed of crystalline rocks, and the Valley and Ridge and Appalachian Plateaus Provinces contain both carbonate and clastic rocks. Annual precipitation ranges from about 36 in. to more than 60 in., and is orographically affected, both locally and regionally. Average annual air temperature ranges from about 43?F to about 55?F, and varies with altitude but not physiographic province. Precipitation is greatest in the summer and least in the winter, and has the least seasonal variation in the Blue Ridge Province.\r\n\r\nIn 1990, the population of the basin was about 870,000, of whom about 25 percent lived in the Charleston, W. Va. metropolitan area. About 75 million tons of coal were mined in the Kanawha River Basin in 1998. This figure represents about 45 percent of the coal mined in West Virginia, and about seven percent of the coal mined in the United States. Dominant forest types in the basin are Northern Hardwood, Oak-Pine, and Mixed Mesophytic. Agricultural land use is more common in the Valley and Ridge and Blue Ridge Provinces than in the Appalachian Plateaus Province. Cattle are the principal agricultural products of the basin.\r\n\r\nStreams in the Blue Ridge Province and Allegheny Highlands have the most runoff in the basin, and streams in the Valley and Ridge Province and the southwestern Appalachian Plateaus have the least runoff. Streamflow is greatest in the spring and least in the autumn. About 61 percent of the basin's population use surface water from public supply for their domestic needs; about 30 percent use self-supplied ground water, and about nine percent use ground water from public supply. In 1995, total withdrawal of water in the basin was about 1,130 Mgal/d. Total consumptive use was about 118 Mgal/d. Surface water in the Blue Ridge Province is usually dilute (less than 100 mg/L dissolved solids) and well aerated. Dissolved- solids concentrations in streams of the Valley and Ridge Province at low flow are typically greater (150-180 mg/L) than those in the Blue Ridge Province. The Appalachian Plateaus Province contains streams with the most dilute (less than 30 mg/L dissolved solids) and least dilute (more than 500 mg/L dissolved solids) water in the basin.\r\n\r\nCoal mining has degraded more miles of streams in the basin than any other land use. Streams that receive coal-mine drainage may be affected by sedimentation, and typically contain high concentrations of sulfate, iron, and manganese. Other major water-quality issues include inadequate domestic sewage treatment, present and historic disposal of industrial wastes, and logging, which results in the addition of sediment, nutrients, and other constituents to the water.\r\n\r\nOne hundred eighteen fish species are reported from the Kanawha River system downstream from Kanawha Falls. Of these, 15 are listed as possible, probable, or known introductions. None of these fish species is endemic to the Kanawha River Basin. The New River system has only 46 native fishes, the lowest ratio of native fishes to drainage area of any river system in the eastern United States, and the second-highest proportion of endemic fish species (eight of 46) of any river system in the eastern United States.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri004020","usgsCitation":"Messinger, T., and Hughes, C., 2000, Environmental setting and its relations to water quality in the Kanawha River basin: U.S. Geological Survey Water-Resources Investigations Report 2000-4020, vii, 57 p. :ill., maps (some col.) ;28 cm., https://doi.org/10.3133/wri004020.","productDescription":"vii, 57 p. :ill., maps (some col.) ;28 cm.","costCenters":[],"links":[{"id":159208,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2274,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri004020/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65dacb","contributors":{"authors":[{"text":"Messinger, Terence 0000-0003-4084-9298 tmessing@usgs.gov","orcid":"https://orcid.org/0000-0003-4084-9298","contributorId":2717,"corporation":false,"usgs":true,"family":"Messinger","given":"Terence","email":"tmessing@usgs.gov","affiliations":[{"id":642,"text":"West Virginia Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200252,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hughes, C.A.","contributorId":13278,"corporation":false,"usgs":true,"family":"Hughes","given":"C.A.","email":"","affiliations":[],"preferred":false,"id":200253,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":24829,"text":"ofr00390 - 2000 - Research, methodology, and applications of probabilistic seismic-hazard mapping of the Central and Eastern United States; minutes of a workshop on June 13-14, 2000, at Saint Louis University","interactions":[],"lastModifiedDate":"2017-03-07T11:02:51","indexId":"ofr00390","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2000-390","title":"Research, methodology, and applications of probabilistic seismic-hazard mapping of the Central and Eastern United States; minutes of a workshop on June 13-14, 2000, at Saint Louis University","docAbstract":"The U.S. Geological Survey (USGS) is updating and revising its 1996 national seismic-hazard maps for release in 2001. Part of this process is the convening of four regional workshops with earth scientists and other users of the maps. The second of these workshops was sponsored by the USGS and the Mid-America Earthquake Center, and was hosted by Saint Louis University on June 13-14, 2000.
The workshop concentrated on the central and eastern U.S. (CEUS) east of the Rocky Mountains. The tasks of the workshop were to (1) evaluate new research findings that are relevant to seismic hazard mapping, (2) discuss modifications in the inputs and methodology used in the national maps, (3) discuss concerns by engineers and other users about the scientific input to the maps and the use of the hazard maps in building codes, and (4) identify needed research in the CEUS that can improve the seismic hazard maps and reduce their uncertainties.
These minutes summarize the workshop discussions. This is not a transcript; some individual remarks and short discussions of side issues and logistics were omitted. Named speakers were sent a draft of the minutes with a request for corrections of any errors in remarks attributed to them. Nine people returned corrections, amplifications, or approvals of their remarks as reported. The rest of this document consists of the meeting agenda, discussion summaries, and a list of the 60 attendees.
","language":"English","publisher":"U.S. Department of the Interior, U.S. Geological Survey,","publisherLocation":"Reston, VA","doi":"10.3133/ofr00390","issn":"0094-9140","usgsCitation":"Wheeler, R.L., and Perkins, D.M., 2000, Research, methodology, and applications of probabilistic seismic-hazard mapping of the Central and Eastern United States; minutes of a workshop on June 13-14, 2000, at Saint Louis University: U.S. Geological Survey Open-File Report 2000-390, 18 p., https://doi.org/10.3133/ofr00390.","productDescription":"18 p.","costCenters":[],"links":[{"id":157127,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2000/0390/report-thumb.jpg"},{"id":53833,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2000/0390/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":1848,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2000/ofr-00-0390/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62c3b0","contributors":{"authors":[{"text":"Wheeler, Russell L. wheeler@usgs.gov","contributorId":858,"corporation":false,"usgs":true,"family":"Wheeler","given":"Russell","email":"wheeler@usgs.gov","middleInitial":"L.","affiliations":[],"preferred":false,"id":192640,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Perkins, David M. perkins@usgs.gov","contributorId":2114,"corporation":false,"usgs":true,"family":"Perkins","given":"David","email":"perkins@usgs.gov","middleInitial":"M.","affiliations":[{"id":301,"text":"Geologic Hazards Team","active":false,"usgs":true}],"preferred":true,"id":192641,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":27861,"text":"wri934167 - 2000 - Water resources of the Blackstone River basin, Massachusetts","interactions":[],"lastModifiedDate":"2018-01-11T14:04:58","indexId":"wri934167","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","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":"93-4167","title":"Water resources of the Blackstone River basin, Massachusetts","docAbstract":"By 2020, demand for water in the Blackstone River Basin is expected to be 52 million gallons per day, one-third greater than the demand of 39 million gallons per day in 1980. Most of this increase is expected to be supplied by increased withdrawals of ground water from stratified-drift aquifers in the eastern and northern parts of the basin. Increased withdrawals from stratified-drift aquifers along the Blackstone River and in the western part of the basin also are expected.
The eastern and northern parts of the Blackstone River Basin contain numerous small, discontinuous aquifers which, as a group, comprise the largest ground-water resource of the study area. Fifteen aquifers, ranging in areal extent from 0.57 to 4.3 square miles, were identified. These aquifers have maximum saturated thicknesses ranging from less than 10 feet to 105 feet and maximum transmissivities ranging from less than 1,000 to more than 20,000 feet squared per day. Yields of nine study aquifers were estimated by use of digital ground-water-flow models. Yields depend on the hydraulic properties of the aquifer and the amount of streamflow available for depletion by wells. If streamflow is maintained at 98-percent duration, long-term yields from the aquifers that would be expected to be equaled or exceeded 50 percent of the time range from 0.22 to 11 million gallons per day, and long-term yields equaled or exceeded 95 percent of the time range from 0.06 to 1.0 million gallons per day. If streamflow is maintained at 99.5-percent duration, long-term yields equaled or exceeded 50 percent of the time range from 0.22 to 11 million gallons per day, long-term yields equaled or exceeded 95 percent of the time range from 0.04 to 1.4 million gallons per day, and longterm yields equaled or exceeded 98 percent of the time range from 0.02 to 0.39 million gallons per day. Maintaining streamflow at 98-percent duration is a more restrictive criterion than maintaining streamflow at 99.5-percent duration.
The upper Lake Quinsigamond, upper West River, and Stone Brook aquifers are capable of sustaining withdrawals of at least 1 million gallons per day more than their rates in the mid-1980s. The upper Mill River and Auburn aquifers are not capable of sustaining additional withdrawals of 0.25 million gallons per day. Ground-water quality in the Auburn aquifer has been degraded by activities and contaminants associated with urbanization.
A nearly continuous deposit of stratified drift almost 30 miles long and from 400 feet to more than 1 mile wide occupies lowland areas along the southeastern part of the Blackstone River. These deposits were divided into four aquifers ranging in areal extent from 1.8 to 3.5 square miles. These aquifers have maximum saturated thicknesses ranging from 54 to 170 feet and maximum transmissivities ranging from less than 1,500 to more than 20,000 feet squared per day. The Blackstone River receives substantial amounts of treated municipal wastewater. Infiltration of poor-quality surface water has significantly increased the specific conductance and the concentrations of all major ions, ammonia, iron, and manganese in the water pumped from at least two wells near the river. These wells derive about 41 and 48 percent of their yield from infiltrated surface water. At both sites, aquifer heterogeneity controlled the movement of infiltrated water to the wells. At one of these sites, where the flow of infiltrated water was tracked (by use of a digital model) in three dimensions, infiltrated water moved to the well through gravel layers that did not constitute the entire thickness of the aquifer. Changes in stream discharge that resulted in changes in surface-water quality also affected the quality of ground water at that site.
The western part of the Blackstone River Basin contains the smallest aquifers evaluated in the study area. Six aquifers, ranging in areal extent from 0.05 to 1.3 square miles, were identified. The hydraulic properties of most of these aquifers have not been determined, but available data indicate that maximum saturated thicknesses range from 28 to 71 feet and maximum transmissivities range from 2,300 to 15,000 feet squared per day.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri934167","collaboration":"Prepared in cooperation with the Massachusetts Department of Environmental Management, Office of Water Resources","usgsCitation":"Izbicki, J., 2000, Water resources of the Blackstone River basin, Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 93-4167, Report: vi, 115 p.; 2 Plates: 46.47 x 34.00 inches and 46.67 x 34.00, https://doi.org/10.3133/wri934167.","productDescription":"Report: vi, 115 p.; 2 Plates: 46.47 x 34.00 inches and 46.67 x 34.00","costCenters":[],"links":[{"id":56684,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1993/4167/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":119867,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1993/4167/report-thumb.jpg"},{"id":350422,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1993/4167/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":350421,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1993/4167/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"48000","country":"United States","state":"Massachusetts","otherGeospatial":"Blackstone River Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.93367004394531,\n 41.9\n ],\n [\n -71.3,\n 41.9\n ],\n [\n -71.3,\n 42.371227435069805\n ],\n [\n -71.93367004394531,\n 42.371227435069805\n ],\n [\n -71.93367004394531,\n 41.9\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f05ec","contributors":{"authors":[{"text":"Izbicki, John A. 0000-0003-0816-4408 jaizbick@usgs.gov","orcid":"https://orcid.org/0000-0003-0816-4408","contributorId":1375,"corporation":false,"usgs":true,"family":"Izbicki","given":"John A.","email":"jaizbick@usgs.gov","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":198801,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28939,"text":"wri994291 - 2000 - Site Selection for a Deep Monitor Well, Kualapuu, Molokai, Hawaii","interactions":[],"lastModifiedDate":"2012-03-08T17:16:15","indexId":"wri994291","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","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":"99-4291","title":"Site Selection for a Deep Monitor Well, Kualapuu, Molokai, Hawaii","docAbstract":"Management of the ground-water resources near Kualapuu on the island of Molokai, Hawaii, is hindered by the uncertainty in the vertical salinity structure in the aquifer. In the State of Hawaii, vertical profiles of ground-water salinity are commonly obtained from deep monitor wells, and these profiles are used to estimate the thicknesses of the freshwater part of the ground-water flow system and the freshwater-saltwater transition zone. Information from a deep monitor well would improve the understanding of the ground-water flow system and the ability to effectively manage the ground-water resources near Kualapuu; however, as of mid-1999 no deep monitor wells had been drilled on the island of Molokai. \r\n\r\nSelection of an appropriate site for drilling a deep monitor well in the Kualapuu area depends partly on where future ground-water development may occur. Simulations using an areally two-dimensional, steady-state, sharp-interface ground-water flow model previously developed for the island of Molokai, Hawaii, indicate that the southeastern part of the Kualapuu area is a possible area of future ground-water development because (1) withdrawals from this area have a small effect on water levels at existing wells in the Kualapuu area (relative to effects from withdrawals in other parts of the Kualapuu area that are outside of the dike complex), and (2) model-calculated water levels in this part of the Kualapuu area are high relative to water levels in other parts of the Kualapuu area that are outside of the dike complex. \r\n\r\nAdditional site-selection criteria include (1) ground-water level, (2) ground-surface altitude, (3) land classification, ownership, and accessibility, (4) geology, (5) locations of existing production wells, and (6) historical ground-water quality information. A deep monitor well in the Kualapuu area will likely be most useful for management purposes if it is located (1) in the vicinity of future ground-water development, (2) in an area where water levels are between about 8 and 12 feet above sea level, (3) at a ground-surface altitude that is between about 1,000 and 1,100 feet, (4) on government-owned land, (5) outside of the dike complex and as far from known volcanic vents as possible, (6) at least about 1,000 feet from, but within the same hydrogeologic setting as, existing or proposed production wells, and (7) east of well 0902-01. A viable area for drilling a deep monitor well is about a half mile southeast of existing wells 0801-01 to -03 and a half mile north of a known volcanic vent, Puu Luahine.","language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/wri994291","usgsCitation":"Oki, D.S., 2000, Site Selection for a Deep Monitor Well, Kualapuu, Molokai, Hawaii: U.S. Geological Survey Water-Resources Investigations Report 99-4291, vi, 50 p., https://doi.org/10.3133/wri994291.","productDescription":"vi, 50 p.","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":95733,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4291/report.pdf","size":"10061","linkFileType":{"id":1,"text":"pdf"}},{"id":158310,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4291/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e486fe4b07f02db50c94e","contributors":{"authors":[{"text":"Oki, Delwyn S. 0000-0002-6913-8804 dsoki@usgs.gov","orcid":"https://orcid.org/0000-0002-6913-8804","contributorId":1901,"corporation":false,"usgs":true,"family":"Oki","given":"Delwyn","email":"dsoki@usgs.gov","middleInitial":"S.","affiliations":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200649,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":45135,"text":"pp1628 - 2000 - Regional ground-water evapotranspiration and ground-water budgets, Great Basin, Nevada","interactions":[],"lastModifiedDate":"2022-07-11T21:21:03.003777","indexId":"pp1628","displayToPublicDate":"2001-06-01T00:00:00","publicationYear":"2000","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1628","title":"Regional ground-water evapotranspiration and ground-water budgets, Great Basin, Nevada","docAbstract":"PART A: Ground-water evapotranspiration data from five sites in Nevada and seven sites in Owens Valley, California, were used to develop equations for estimating ground-water evapotranspiration as a function of phreatophyte plant cover or as a function of the depth to ground water. Equations are given for estimating mean daily seasonal and annual ground-water evapotranspiration. The equations that estimate ground-water evapotranspiration as a function of plant cover can be used to estimate regional-scale ground-water evapotranspiration using vegetation indices derived from satellite data for areas where the depth to ground water is poorly known. Equations that estimate ground-water evapotranspiration as a function of the depth to ground water can be used where the depth to ground water is known, but for which information on plant cover is lacking. \r\n\r\nPART B: Previous ground-water studies estimated groundwater evapotranspiration by phreatophytes and bare soil in Nevada on the basis of results of field studies published in 1912 and 1932. More recent studies of evapotranspiration by rangeland phreatophytes, using micrometeorological methods as discussed in Chapter A of this report, provide new data on which to base estimates of ground-water evapotranspiration. An approach correlating ground-water evapotranspiration with plant cover is used in conjunction with a modified soil-adjusted vegetation index derived from Landsat data to develop a method for estimating the magnitude and distribution of ground-water evapotranspiration at a regional scale. Large areas of phreatophytes near Duckwater and Lockes in Railroad Valley are believed to subsist on ground water discharged from nearby regional springs. Ground-water evapotranspiration by the Duckwater phreatophytes of about 11,500 acre-feet estimated by the method described in this report compares well with measured discharge of about 13,500 acre-feet from the springs near Duckwater. Measured discharge from springs near Lockes was about 2,400 acre-feet; estimated ground-water evapotranspiration using the proposed method was about 2,450 acre-feet. \r\n\r\nPART C: Previous estimates of ground-water budgets in Nevada were based on methods and data that now are more than 60 years old. Newer methods, data, and technologies were used in the present study to estimate ground-water recharge from precipitation and ground-water discharge by evapotranspiration by phreatophytes for 16 contiguous valleys in eastern Nevada. Annual ground-water recharge to these valleys was estimated to be about 855,000 acre-feet and annual ground-water evapotranspiration was estimated to be about 790,000 acrefeet; both are a little more than two times greater than previous estimates. The imbalance of recharge over evapotranspiration represents recharge that either (1) leaves the area as interbasin flow or (2) is derived from precipitation that falls on terrain within the topographic boundary of the study area but contributes to discharge from hydrologic systems that lie outside these topographic limits. \r\n\r\nA vegetation index derived from Landsat-satellite data was used to estimate phreatophyte plant cover on the floors of the 16 valleys. The estimated phreatophyte plant cover then was used to estimate annual ground-water evapotranspiration. Detailed estimates of summer, winter, and annual ground-water evapotranspiration for areas with different ranges of phreatophyte plant cover were prepared for each valley. The estimated ground-water discharge from 15 valleys, combined with independent estimates of interbasin ground-water flow into or from a valley, were used to calculate the percentage of recharge derived from precipitation within the topographic boundary of each valley. These percentages then were used to estimate ground-water recharge from precipitation within each valley. \r\n\r\nGround-water budgets for all 16 valleys were based on the estimated recharge from precipitation and estimated evapotranspiration. Any imba","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1628","usgsCitation":"Nichols, W., 2000, Regional ground-water evapotranspiration and ground-water budgets, Great Basin, Nevada: U.S. Geological Survey Professional Paper 1628, Report: 101 p.; 4 Plates: 30.00 × 60.00 inches or smaller, https://doi.org/10.3133/pp1628.","productDescription":"Report: 101 p.; 4 Plates: 30.00 × 60.00 inches or smaller","costCenters":[],"links":[{"id":403440,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_34830.htm","linkFileType":{"id":5,"text":"html"}},{"id":336793,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1628/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":120215,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1628/report-thumb.jpg"},{"id":82270,"rank":302,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1628/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247729,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1628/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247727,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1628/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247728,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1628/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nevada","otherGeospatial":"Great Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.567,\n 38\n ],\n [\n -114.204,\n 38\n ],\n [\n -114.204,\n 41.133\n ],\n [\n -116.567,\n 41.133\n ],\n [\n -116.567,\n 38\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4792e4b07f02db48bd33","contributors":{"authors":[{"text":"Nichols, William D.","contributorId":98296,"corporation":false,"usgs":true,"family":"Nichols","given":"William D.","affiliations":[],"preferred":false,"id":231170,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":25465,"text":"wri994246 - 2000 - Effects of land use and hydrogeology on the water quality of alluvial aquifers in eastern Iowa and southern Minnesota, 1997","interactions":[],"lastModifiedDate":"2016-02-10T14:33:02","indexId":"wri994246","displayToPublicDate":"2001-05-01T00:00:00","publicationYear":"2000","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":"99-4246","title":"Effects of land use and hydrogeology on the water quality of alluvial aquifers in eastern Iowa and southern Minnesota, 1997","docAbstract":"Ground-water samples were collected from monitoring wells at 31 agricultural and 30 urban sites in the Eastern Iowa Basins study unit during June–August 1997 to evaluate the effects of land use and hydrogeology on the water quality of alluvial aquifers. Ground-water samples were analyzed for common ions, nutrients, dissolved organic carbon, tritium, radon-222, pesticides and pesticide metabolites, volatile organic compounds, and environmental isotopes.
\nCalcium, magnesium, and bicarbonate were the dominant ions in most samples and were likely derived from solution of carbonate minerals (calcite and dolomite) present in alluvial detrital deposits. Chloride and nitrate were dominant anions in samples from several wells. Sodium and chloride concentrations were significantly higher in samples from urban areas, where roads are more numerous and road salts may be more frequently applied, than in agricultural areas. Nitrate was detected in 94 percent of samples from agricultural areas and 77 percent of samples from urban areas. Nitrate concentrations were significantly higher in agricultural areas than in urban areas and exceeded the U.S. Environmental Protection Agency maximum ontaminant level for drinking water (10 milligrams per liter as N) in 39 percent of samples from agricultural areas. Nitrate concentrations in samples from urban areas did not exceed the maximum contaminant level. Greater use of fertilizers in agricultural areas most likely contributes to higher nitrate concentrations in samples from those areas.
\nTritium-based ages indicate ground water was most likely recharged after the 1950’s at all but one sampling site. Agricultural and urban land-use areas have remained relatively stable in the study area since the 1950’s; therefore, the effects of current land use should be reflected in ground water sampled during this study. Radon-222 was detected in all samples and exceeded the U.S. Environmental Protection Agency’s previously proposed maximum contaminant level for drinking water (300 picocuries per liter) in 71 percent of samples.
\nPesticides were detected in 84 percent of samples from agricultural areas and 70 percent from urban areas. Atrazine and metolachlor were the most frequently detected pesticides in samples from agricultural areas; atrazine and prometon were the most frequently detected pesticides in samples from urban areas. None of the pesticide oncentrations exceeded U.S. Environmental Protection Agency maximum contaminant levels or lifetime health advisories for drinking water. Pesticide metabolites were detected in 94 percent of samples from agricultural areas and 53 percent from urban areas. Metolachlor ethane sulfonic acid and deethylatrazine were the most frequently detected metabolites in samples from agricultural areas; metolachlor ethane sulfonic acid and alachlor ethane sulfonic acid were the most frequently detected metabolites in samples from urban areas.
\nTotal metabolite concentrations were significantly higher in samples from agricultural areas than in samples from urban areas. Total pesticide concentrations (parent compounds) tended to be higher in samples from agricultural areas; however, this difference was not statistically significant.
\nMetabolites constituted the major portion of the total residue concentration in the alluvial aquifer.
\nVolatile organic compounds were detected in 40 percent of samples from urban areas and 10 percent from agricultural areas. Methyl tertbutyl ether was the most commonly detected volatile organic compound and was present in 23 percent of samples from urban areas. Elevated concentrations (greater than 30 micrograms per liter) of methyl tert-butyl ether and BTEX compounds (benzene, toluene, ethylbenzene, and xylene) in two samples from urban areas suggest the possible presence of point-source gasoline leaks or spills.
\nFactors other than land use may contribute to observed differences in water quality between and within agricultural and urban areas. Nitrate, atrazine, deethylatrazine, and deisopropylatrazine concentrations were significantly higher in shallow wells with sample intervals nearer the water table and in wells with thinner cumulative clay thickness above the sample intervals. These relations suggest that longer flow paths allow for greater residence time and increase opportunities for sorption, degradation, and dispersion, which may contribute to decreases in nutrient and pesticide concentrations with depth. Nitrogen speciation was influenced by redox conditions. Nitrate concentrations were significantly higher in ground water with dissolved-oxygen concentrations in excess of 0.5 milligram per liter. Ammonia concentrations were higher in ground water with dissolved-oxygen concentrations of 0.5 milligram per liter or less; however, this relation was not statistically significant. The amount of available organic matter may limit denitrification rates. Elevated nitrate concentrations (greater than 2.0 mg/L) were significantly related to lower dissolved organic carbon concentrations in water samples from both agricultural and urban areas. A similar relation between nitrate concentrations (in water) and organic carbon concentrations (in aquifer material) also was observed but was not statistically significant.
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