Siting of waste-disposal facilities in Cortland County poses a potential threat to local ground-water resources. An especially sensitive waste-disposal siting issue arose in 1988, when the New York State Low-Level Radioactive Waste Siting Commission (NYSLLWSC) identified 15 sites in six towns (Towns of Solon, Taylor, Freetown, Cincinnatus, Marathon, and Willet) in the eastern part of the county for possible disposal of low-level radioactive waste (New York State Low-Level Radioactive Waste Siting Commission, 1988). Eventually, two sites in the Town of Taylor became finalist sites; one was selected from the list of 15 potential sites, and the other was offered by a private landowner. Little information was available on geohydrologic conditions in eastern Cortland County, such as the extent of aquifers and the thickness of unconsolidated deposits of low permeability (such as clay and till), even though these two criteria were among those used by NYSLLWSC for selection of potential disposal sites. The source of information on thickness of drift over bedrock was the surficial geologic map of New York (Muller and Cadwell, 1986). The siting effort was terminated before a final selection was made, but the issue had made county managers aware that detailed information on the extent and thickness of unconsolidated deposits (particularly till, which typically has low permeability and can limit the migration of contaminants) is needed before sound decisions on waste-disposal siting can be made.
Glaciers deposited till nearly everywhere over bedrock in the uplands of central New York, but the thickness of the till varies greatly from place to place. An analysis by Coates (1966) of 400 drillers' logs of wells in a 2,000-mi2 area in the uplands of south-central New York (south of the Cortland County) indicated that (1) till is thin or absent on hilltops and is thickest on the lower parts of hills, (2) overall till thickness averages 60 ft, and (3) till thickness on the south, east, west, and north slopes averages 92, 52, 62, and 22 ft, respectively. Hills that have thick till on their south slopes have been referred to as till-shadowed hills by Coates (1974), who attributes this characteristic to glaciers that deposited thick amounts of till on the downflow side of a hill (analogous to flowing streams or wind that deposit sediment on the lee side of an object). Because the till on the south slopes is relatively thick and typically has low permeability, these slopes have been considered as potential areas for waste-disposal sites.
In 1997, the U.S. Geological Survey (USGS), in cooperation with the Cortland County Department of Planning, began a 1-year study to map the thickness of unconsolidated deposits and the extent of valley-fill aquifers in the Towns of Solon and Taylor (an area of 60 mi2) in eastern Cortland County.
This report (1) depicts the thickness of unconsolidated deposits and the extent of valley-fill aquifers in the Towns of Solon and taylor in eastern Cortland County, (2) examines whether the \"till-shadowed hill\" concept developed by Coates (1966) is applicable in this area, and (3) provides three schematic geologic sections showing the thickness of unconsolidated deposits in the uplands in the northwestern part of the study area.
","language":"English","publisher":" U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri984197","collaboration":"Prepared in cooperation with the Cortland County Department of Planning","usgsCitation":"Miller, T.S., 1999, Thickness of unconsolidated deposits in the towns of Solon and Taylor, Cortland County, New York: U.S. Geological Survey Water-Resources Investigations Report 98-4197, 40 x 28 inches, https://doi.org/10.3133/wri984197.","productDescription":"40 x 28 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":3229,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1998/4197/wri19984197.pdf","text":"Report","size":"19 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 1998-4197"},{"id":124918,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1998/4197/coverthb.jpg"}],"country":"United States","state":"New York","county":"Cortland County","city":"Solon, Taylor","contact":"Director, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
This site provides information about the number, thickness, and grainsize of Holocene volcanic ash deposits at 50 localities in the eastern Aleutian volcanic arc. In addition, the major-element compositions of the glasses separated from more than 350 samples of tephra from these localities, determined by electron microprobe, are presented as a basis for correlating samples. Where known with reasonable certainty, the source of an analyzed sample is also identified for use in comparative studies of magma chemistry.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr99135","issn":"0094-9140","usgsCitation":"Riehle, J., Meyer, C., and Miyaoka, R.T., 1999, Data on Holocene tephra (volcanic ash) deposits in the Alaska Peninsula and lower Cook Inlet region of the Aleutian volcanic arc, Alaska: U.S. Geological Survey Open-File Report 99-135, HTML Document, https://doi.org/10.3133/ofr99135.","productDescription":"HTML Document","costCenters":[{"id":121,"text":"Alaska Volcano Observatory","active":false,"usgs":true}],"links":[{"id":157417,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":9929,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://kiska.giseis.alaska.edu/dbases/akpen_tephra/akpen_tephra.html","linkFileType":{"id":5,"text":"html"}},{"id":1695,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://avo.alaska.edu/downloads/reference.php?citid=819","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -162,56 ], [ -162,62 ], [ -150,62 ], [ -150,56 ], [ -162,56 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c87d","contributors":{"authors":[{"text":"Riehle, J.R.","contributorId":73573,"corporation":false,"usgs":true,"family":"Riehle","given":"J.R.","affiliations":[],"preferred":false,"id":191698,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Meyer, C.E.","contributorId":104023,"corporation":false,"usgs":true,"family":"Meyer","given":"C.E.","email":"","affiliations":[],"preferred":false,"id":191699,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Miyaoka, Ronny T.","contributorId":61861,"corporation":false,"usgs":true,"family":"Miyaoka","given":"Ronny","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":191697,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":24879,"text":"ofr99317 - 1999 - Digital data for the geologic framework of the Alaska Peninsula, southwest Alaska, and the Alaska Peninsula terrane","interactions":[],"lastModifiedDate":"2022-06-27T19:29:59.101009","indexId":"ofr99317","displayToPublicDate":"2002-01-01T00:00:00","publicationYear":"1999","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":"99-317","title":"Digital data for the geologic framework of the Alaska Peninsula, southwest Alaska, and the Alaska Peninsula terrane","docAbstract":"These digital databases are the result of the compilation and reinterpretation of published and unpublished 1:250,000- and 1:63,360-scale mapping. The map area covers approximately 62,000 sq km (23,000 sq mi) in land area and encompasses much of 13 1:250,000-scale quadrangles on the Alaska Peninsula in southwestern Alaska. The compilation was done as part of the U.S. Geological Survey's Alaska Mineral Resource Assessment project (AMRAP), whose goal was create and assemble geologic, geochemical, geophysical, and other data in order to perform mineral resource assessments on a quadrangle, regional or statewide basis. The digital data here was created to assist in the completion of a regional mineral resource assessment of the Alaska Peninsula.
Mapping on the Alaska Peninsula under AMRAP began in 1977 in the Chignik and Sutwik Island 1:250,000 quadrangles (Detterman and others, 1981). Continued mapping in the Ugashik, bristol bay, and northwestern Karluk quadrangles (Detterman and others, 1987) began in 1979, followed by the Mount Katmai, eastern Naknek, and northwestern Afognak quadrangles (Riehle and others, 1987; Riehle and others, 1993), the Port Moller, Stepovak bay, and Simeonof Island quadrangles (Wilson and others, 1995) beginning in 1983. Work in the Cold bay and False Pass quadrangles (Wilson and others, 1992 [Superseded by Wilson and others 1997, but not incorporated herein]) began in 1986.
The reliability of the geologic mapping is variable, based, in part, on the field time spent in each area of the map, the available support, and the quality of the existing base maps. In addition, our developing understanding of the geology of the Alaska Peninsula required revision of earlier maps, such as the Chignik and Sutwik Island quadrangles map (Detterman and others, 1981) to reflect this new knowledge. We have revised the stratigraphic nomenclature (Detterman and others, 1996) and our assignment of unit names to some rocks has been changed.
All geologic maps on which this compilation is based were published using the Universal Transverse Mercator projection (UTM; Zones 3, 4, and 5). because of the distortions use of the UTM projection would produce on a map of small scale and large area, the plot and graphics files derived from this data are plotted using a more appropriate Albers Equal-area projection for publication.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr99317","issn":"0094-9140","usgsCitation":"Wilson, F.H., Detterman, R.L., and DuBois, G.D., 1999, Digital data for the geologic framework of the Alaska Peninsula, southwest Alaska, and the Alaska Peninsula terrane: U.S. Geological Survey Open-File Report 99-317, Report: 41 p.; 1 Plate: 60.0 x 43.0 inches; Readme; Metadata, https://doi.org/10.3133/ofr99317.","productDescription":"Report: 41 p.; 1 Plate: 60.0 x 43.0 inches; Readme; Metadata","numberOfPages":"43","additionalOnlineFiles":"Y","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":157649,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr99317.jpg"},{"id":1872,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1999/0317/","linkFileType":{"id":5,"text":"html"}},{"id":284894,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/of/1999/0317/akpenrdme.txt"},{"id":109903,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_23296.htm","linkFileType":{"id":5,"text":"html"},"description":"23296"},{"id":284897,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1999/0317/pdf/akpen.pdf"},{"id":284896,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1999/0317/pdf/aptext.pdf"},{"id":284895,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/of/1999/0317/akpenmet.txt"}],"scale":"500000","projection":"Albers Equal Area projection","country":"United States","state":"Alaska","otherGeospatial":"Alaska Peninsula","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -165.02,53.98 ], [ -165.02,59.13 ], [ -153.11,59.13 ], [ -153.11,53.98 ], [ -165.02,53.98 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd54f6e4b0b290850f60e6","contributors":{"authors":[{"text":"Wilson, Frederic H. 0000-0003-1761-6437 fwilson@usgs.gov","orcid":"https://orcid.org/0000-0003-1761-6437","contributorId":67174,"corporation":false,"usgs":true,"family":"Wilson","given":"Frederic","email":"fwilson@usgs.gov","middleInitial":"H.","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":192729,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Detterman, Robert L.","contributorId":71526,"corporation":false,"usgs":true,"family":"Detterman","given":"Robert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":192731,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"DuBois, Gregory D.","contributorId":6824,"corporation":false,"usgs":true,"family":"DuBois","given":"Gregory","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":192730,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":31109,"text":"ofr97639 - 1999 - Hydrogeology of the Schodack-Kinderhook Area, Rensselaer and Columbia Counties, New York","interactions":[],"lastModifiedDate":"2022-08-17T19:57:53.578464","indexId":"ofr97639","displayToPublicDate":"2001-12-01T00:00:00","publicationYear":"1999","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":"97-639","title":"Hydrogeology of the Schodack-Kinderhook Area, Rensselaer and Columbia Counties, New York","docAbstract":"Two glaciodeltaic outwash terraces in southern Rensselaer and northern Columbia Counties, known locally as the Schodack and Kinderhook terraces, consist of ice-contact and outwash sand and gravel and together form a regional, unconfined, stratified-drift aquifer with a combined area of 18.75 square miles. The hydrogeology of these aquifers is summarized on four maps at 1:24,000 scale, that depict (1) locations of wells and test holes, (2) surficial geology, (3) altitude of the water table, and (4) altitude of the bedrock surface.
Both terraces are associated with a thin and probably discontinuous confined aquifer consisting of beds of glaciofluvial sand and gravel derived from the outwash deltas that form the two terraces. The confined aquifer is overlain by thick deposits of lacustrine silt and clay. Consultants? estimates of average hydraulic conductivity, based on aquifer tests conducted at four test wells screened in thicker sections of the confined aquifer, range from 430 to 2,360 ft/d (feet per day), with a mean of 1,150 ft/d. The mean estimate of hydraulic conductivity derived from specific-capacity data from 16 test wells screened in confined and unconfined sections of the aquifer is 640 ft/d.
Reported yields for domestic wells completed in unconfined sections of the Schodack and Kinderhook terrace aquifers average 16.1 and 18.3 gal/min (gallons per minute), respectively, and reported yields of domestic wells completed in hydraulically confined sections of these terraces average 15.3 and 12.8 gal/ min, respectively. Yields from public-supply wells screened in the confined sections of the Schodack Terrace aquifer range from 50 to 1,050 gal/min and average 305 gal/min. Average annual recharge to the Schodack Terrace aquifer and adjacent upland till deposits, as estimated in a 1960 U.S. Geological Survey study, were 16.3 and 7.1 inches per square mile, respectively. Bedrock that underlies the study area has been highly modified by tectonic activity, differential weathering, and preglacial erosion which produced about 900 ft of relief on the bedrock surface. A major thrust fault that runs north-south through the area separates autocthonous Ordovician rock units to the west from allocthonous Cambrian (Taconic) rocks to the east.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr97639","collaboration":"Prepared in cooperation with the New York Department of Environmental Conservation","usgsCitation":"Reynolds, R.J., 1999, Hydrogeology of the Schodack-Kinderhook Area, Rensselaer and Columbia Counties, New York: U.S. Geological Survey Open-File Report 97-639, Report: iv, 73 p.; 8 Plates: 32.17 × 52.15 inches or smaller, https://doi.org/10.3133/ofr97639.","productDescription":"Report: iv, 73 p.; 8 Plates: 32.17 × 52.15 inches or smaller","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":258660,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate4.pdf","text":"Plate 4 - Bedrock-surface altitude","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":326250,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate3big.pdf","text":"Plate 3 - Water-table altitude (larger size)","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":258659,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate3.pdf","text":"Plate 3 - Water-table altitude","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":326249,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate2big.pdf","text":"Plate 2 - Surficial geology (larger size)","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":258658,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate2.pdf","text":"Plate 2 - Surficial geology","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":326229,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate1big.pdf","text":"Plate 1 - Locations of wells and test holes (larger size)","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":258657,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate1.pdf","text":"Plate 1 - Locations of wells and test holes","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":2582,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":326251,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1997/0639/ofr19970639_plate4big.pdf","text":"Plate 4 - Bedrock-surface altitude (larger size)","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 197-0639"},{"id":397738,"rank":11,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_26592.htm","linkFileType":{"id":5,"text":"html"}},{"id":161118,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1997/0639/coverthb.jpg"}],"scale":"24000","country":"United States","state":"New York","county":"Columbia County, Rensselaer County","otherGeospatial":"Schodack - Kinderhook area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.8,\n 42.375\n ],\n [\n -73.625,\n 42.375\n ],\n [\n -73.625,\n 42.5\n ],\n [\n -73.8,\n 42.5\n ],\n [\n -73.8,\n 42.375\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, New York Water Science Center
U.S. Geological Survey
425 Jordan Rd
Troy, NY 12180
(518) 285-5695
http://ny.water.usgs.gov/
Irondequoit Creek, which drains 169 square miles in the eastern part of Monroe County, has been recognized as a source of contaminants that contribute to the eutrophication of Irondequoit Bay on Lake Ontario. The discharge from sewage-treatment plants to the creek and its tributaries was eliminated in 1979 by diversion to another wastewater-treatment facility, but sediment and nonpoint-source pollution remain a concern. This report presents data from five surface-water sites in the Irondequoit Creek basin. Irondequoit Creek at Railroad Mills, East Branch Allen Creek, Allen Creek near Rochester, Irondequoit Creek at Blossom Road, and Irondequoit Creek at Empire Boulevard, to supplement published data from 1984-88. Data from Northrup Creek, which drains 11.7 square miles in western Monroe County, provide information on surface-water quality west of the Genesee River. Also presented are water-level and water-quality data from 12 observation-well sites in Ellison and Powdermill Parks and atmospheric-deposition data from 1 site (Mendon Ponds).
Concentrations of several chemical constituents in streams of the Irondequoit Creek basin showed statistically significant trends during 1989-93. Concentrations of total suspended-solids and volatile suspended-solids in Irondequoit Creek at Blossom Road decreased 13.5 and 12.5 percent per year, respectively, and those at Empire Boulevard decreased 33.5 and 22 percent per year, respectively.
Concentrations of ammonia plus organic nitrogen increased 17.6 percent per year at one site in the basin, but decreased 8.5 and 22.3 percent per year at two sites. Nitrite plus nitrate decreased at only one site (3.5 percent per year). Concentrations of total phosphorus increased at two sites (about 7 percent per year) and decreased at two other sites (7.6 and 29.9 percent per year), and orthophosphate concentrations increased at one site (10.8 percent per year). Dissolved chloride increased at three sites (1.7 to 10.9 percent per year), and dissolved sulfate decreased at one site (2.1 percent per year) and increased at one site (6.8 percent per year).
Median concentrations of constituents were significantly lower in atmospheric deposition than in streamflow, although annual deposition of ammonia nitrogen, nitrite plus nitrate, total phosphorus, and orthophosphate in the basin exceeded the amounts removed by streamflow. Atmospheric deposition of chloride and sulfate, by contrast, represented only 1 and 12 percent, respectively, of the loads transported by Irondequoit Creek (Blossom Road site).
Comparison of water-quality data from the Allen Creek site and Irondequoit Creek at Blossom Road from water years 1989-93 with corresponding data from 1984-88 indicates significant changes in median concentrations of several constituents. The concentration of dissolved chloride increased at Blossom Road and was unchanged at Allen Creek, whereas sulfate decreased at both sites. Concentrations of ammonia plus organic nitrogen, and nitrite plus nitrate, were significantly lower during 1989-93 than during 1984-88 at both sites. Total phosphorus concentration was lower during 1984-88 than during 1989-93 at Blossom Road but showed no change at Allen Creek, and orthophosphate concentration for 1989-93 was lower than in 1984-88 at both sites. Comparison of chemical loads in atmospheric deposition also indicates significant changes in many constituents. Five-year-mean loads of sodium, sulfate, and lead in atmospheric deposition for 1989-93 exceeded those for 1984-88, whereas 5-year-mean loads of calcium, magnesium, potassium, chloride, nitrite plus nitrate, ammonia nitrogen, and orthophosphate for 1989-93 were lower than in 1984-88.
The changes in surface-water quality resulted from several factors within the basin, including land-use changes, annual and seasonal variations in streamflow, and year-to-year variations in the application of deicing salts on area roads. Statistical analyses of long-term (9 years or more) flow records of three unregulated streams in Monroe County indicate that annual mean flows for water years 1989- 93 were in the normal range (20th- to 80th-percentile). The greatest mean annual flow in this period-about 140 percent of normal at Irondequoit Creek and Black Creek-occurred in 1993, but the annual mean flow for that water year at Allen Creek was only 98 percent of normal. The lowest annual mean flows of these streams-ranging from 75 percent of normal to 93 percent of normal-occurred in 1989. The average annual mean flows for these streams for 1989-93 was 104 percent of normal, and that for 1984-88 was normal.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994084","usgsCitation":"Sherwood, D.A., 1999, Water resources of Monroe County, New York, water years 1989-93, with emphasis on water quality in the Irondequoit Creek basin: Part 2. Atmospheric deposition, ground water, streamflow, trends in water quality, and chemical loads to Irondequoit Bay: U.S. Geological Survey Water-Resources Investigations Report 99-4084, v, 50 p., https://doi.org/10.3133/wri994084.","productDescription":"v, 50 p.","costCenters":[],"links":[{"id":410243,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_22770.htm","linkFileType":{"id":5,"text":"html"}},{"id":274647,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4084/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":159511,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4084/report-thumb.jpg"}],"country":"United States","state":"New York","county":"Monroe County","otherGeospatial":"Irondequoit Creek basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -77.625,\n 43.25\n ],\n [\n -77.625,\n 43\n ],\n [\n -77.375,\n 43\n ],\n [\n -77.375,\n 43.25\n ],\n [\n -77.625,\n 43.25\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49b4e4b07f02db5ca5c0","contributors":{"authors":[{"text":"Sherwood, Donald A.","contributorId":103267,"corporation":false,"usgs":true,"family":"Sherwood","given":"Donald","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":201975,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28814,"text":"wri994058 - 1999 - Simulated effects of projected ground-water withdrawals in the Floridan aquifer system, greater Orlando metropolitan area, east-central Florida","interactions":[],"lastModifiedDate":"2012-02-02T00:08:46","indexId":"wri994058","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4058","title":"Simulated effects of projected ground-water withdrawals in the Floridan aquifer system, greater Orlando metropolitan area, east-central Florida","docAbstract":"Ground-water levels in the Floridan aquifer system within the greater Orlando metropolitan area are expected to decline because of a projected increase in the average pumpage rate from 410 million gallons per day in 1995 to 576 million gallons per day in 2020. The potential decline in ground-water levels and spring discharge within the area was investigated with a calibrated, steady-state, ground-water flow model. A wetter-than-average condition scenario and a drought-condition scenario were simulated to bracket the range of water-levels and springflow that may occur in 2020 under average rainfall conditions. Pumpage used to represent the drought-condition scenario totaled 865 million gallons per day, about 50 percent greater than the projected average pumpage rate in 2020. Relative to average 1995 steady-state conditions, drawdowns simulated in the Upper Floridan aquifer exceeded 10 and 25 feet for wet and dry conditions, respectively, in parts of central and southwest Orange County and in north Osceola County. In Seminole County, drawdowns of up to 20 feet were simulated for dry conditions, compared with 5 to 10 feet simulated for wet conditions. Computed springflow was reduced by 10 percent for wet conditions and by 38 percent for dry conditions, with the largest reductions (28 and 76 percent) occurring at the Sanlando Springs group. In the Lower Floridan aquifer, drawdowns simulated in southwest Orange County exceeded 20 and 40 feet for wet and dry conditions, respectively. ","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri994058","usgsCitation":"Murray, L.C., and Halford, K.J., 1999, Simulated effects of projected ground-water withdrawals in the Floridan aquifer system, greater Orlando metropolitan area, east-central Florida: U.S. Geological Survey Water-Resources Investigations Report 99-4058, iv, 26 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri994058.","productDescription":"iv, 26 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":95726,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4058/report.pdf","size":"2969","linkFileType":{"id":1,"text":"pdf"}},{"id":2324,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://fl.water.usgs.gov/Abstracts/wri99_4058_murray.html","linkFileType":{"id":5,"text":"html"}},{"id":159187,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4058/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db69831f","contributors":{"authors":[{"text":"Murray, Louis C. Jr.","contributorId":19980,"corporation":false,"usgs":true,"family":"Murray","given":"Louis","suffix":"Jr.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":200441,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Halford, Keith J. 0000-0002-7322-1846 khalford@usgs.gov","orcid":"https://orcid.org/0000-0002-7322-1846","contributorId":1374,"corporation":false,"usgs":true,"family":"Halford","given":"Keith","email":"khalford@usgs.gov","middleInitial":"J.","affiliations":[{"id":465,"text":"Nevada Water Science Center","active":true,"usgs":true}],"preferred":true,"id":200440,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28726,"text":"wri994062 - 1999 - Water quality in the southern Everglades and Big Cypress Swamp in the vicinity of the Tamiami Trail, 1996-97","interactions":[],"lastModifiedDate":"2017-10-18T11:43:21","indexId":"wri994062","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4062","title":"Water quality in the southern Everglades and Big Cypress Swamp in the vicinity of the Tamiami Trail, 1996-97","docAbstract":"The quality of water flowing southward in the Everglades and Big Cypress Swamp was characterized by three synoptic surveys along an 80-mile section of the Tamiami Trail and along a 24-mile transect down the Shark River Slough, by monthly sampling of a background reference site in the central Big Cypress Swamp, and by sampling of fish tissue for contaminants at several sites near the Trail. The quality of water along the Trail is spatially variable due to natural and human influences. Concentrations of dissolved solids and common ions such as chloride and sulfate were lowest in the central and eastern Big Cypress Swamp and were higher to the west due to the effects of seawater, especially during the dry season, and to the east due to canal drainage from the northern Everglades. Concentrations of total phosphorus tended to decrease from west to east along the 80-mile section of the Trail, and were usually about 0.01 milligram per liter or less in the Everglades. Short-term loads (based on average discharge for 4 days) of total phosphorus and total Kjeldahl nitrogen (ammonia plus organic nitrogen) across four gaged sections of the Tamiami Trail were highest in the Everglades near the S-12 structures primarily due to the relatively greater discharges in that section. Concentrations of dissolved solids and total phosphorus at the central Big Cypress Swamp site increased significantly during the dry season as waters ponded. Effects of nearby, upstream agricultural activities were evident at a site in the western Big Cypress Swamp where relatively high concentrations of total phosphorus, total mercury, and dissolved organic carbon and high periphyton biomass accumulation rates were measured and where several pesticides were detected. The most frequently detected pesticides along the Trail were atrazine (14 detections), tebuthiuron (11 detections), and metolachlor (5 detections), and most concentrations were less than 0.1 microgram per liter. DDT compounds were the only pesticides detected in fish from five sites. Total DDT ranged from 5 to 6 micrograms per kilogram in largemouth bass and from 11 to 17 micrograms per kilogram in Florida gar. ","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994062","usgsCitation":"Miller, R.L., McPherson, B.F., and Haag, K.H., 1999, Water quality in the southern Everglades and Big Cypress Swamp in the vicinity of the Tamiami Trail, 1996-97: U.S. Geological Survey Water-Resources Investigations Report 99-4062, 16 p., https://doi.org/10.3133/wri994062.","productDescription":"16 p.","costCenters":[],"links":[{"id":159142,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2300,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri994062","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.25306701660158,\n 26.324806523453258\n ],\n [\n -80.25306701660158,\n 26.44536920598803\n ],\n [\n -80.35194396972658,\n 26.489625902389264\n ],\n [\n -80.44532775878908,\n 26.526493474751604\n ],\n [\n -80.62660217285158,\n 26.52895089214116\n ],\n [\n -80.75019836425783,\n 26.469958360799367\n ],\n [\n -80.85456848144534,\n 26.337114601297504\n ],\n [\n -80.91773986816409,\n 26.23861337022362\n ],\n [\n -81.13197326660158,\n 26.204118192100207\n ],\n [\n -81.55494689941408,\n 26.20658247256803\n ],\n [\n -81.69570922851562,\n 26.262630753291948\n ],\n [\n -81.81106567382812,\n 26.28356493253137\n ],\n [\n -81.8316650390625,\n 26.278023899612247\n ],\n [\n -81.82891845703125,\n 26.26447803862256\n ],\n [\n -81.82823181152345,\n 26.246003863035007\n ],\n [\n -81.82823181152345,\n 26.228758648862744\n ],\n [\n -81.82411193847658,\n 26.160984843066014\n ],\n [\n -81.82136535644534,\n 26.0808377326361\n ],\n [\n -81.7705535888672,\n 25.98952649069162\n ],\n [\n -81.60987854003908,\n 25.893202651527957\n ],\n [\n -81.58515930175781,\n 25.87343418430102\n ],\n [\n -81.47804260253909,\n 25.821526220975297\n ],\n [\n -81.36268615722658,\n 25.752280195982966\n ],\n [\n -81.28303527832034,\n 25.643383430793335\n ],\n [\n -81.21162414550783,\n 25.489769266691464\n ],\n [\n -81.15669250488283,\n 25.38063344135006\n ],\n [\n -81.08253479003908,\n 25.343405468986074\n ],\n [\n -80.97267150878908,\n 25.363261814488446\n ],\n [\n -80.65132141113283,\n 25.23910621817942\n ],\n [\n -80.57991027832033,\n 25.273882601490126\n ],\n [\n -80.46180725097656,\n 25.44513474341806\n ],\n [\n -80.32722473144533,\n 25.969774178414728\n ],\n [\n -80.25306701660158,\n 26.324806523453258\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f99ef","contributors":{"authors":[{"text":"Miller, Ronald L.","contributorId":103245,"corporation":false,"usgs":true,"family":"Miller","given":"Ronald","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":200299,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McPherson, Benjamin F.","contributorId":17965,"corporation":false,"usgs":true,"family":"McPherson","given":"Benjamin","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":200298,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Haag, Kim H. khhaag@usgs.gov","contributorId":381,"corporation":false,"usgs":true,"family":"Haag","given":"Kim","email":"khhaag@usgs.gov","middleInitial":"H.","affiliations":[],"preferred":true,"id":200297,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":26486,"text":"wri994099 - 1999 - Application of continuous seismic-reflection techniques to delineate paleochannels beneath the Neuse River at U.S. Marine Corps Air Station, Cherry Point, North Carolina","interactions":[],"lastModifiedDate":"2022-01-10T22:21:51.32016","indexId":"wri994099","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4099","title":"Application of continuous seismic-reflection techniques to delineate paleochannels beneath the Neuse River at U.S. Marine Corps Air Station, Cherry Point, North Carolina","docAbstract":"A continuous seismic-reflection profiling survey was conducted by the U.S. Geological Survey on the Neuse River near the Cherry Point Marine Corps Air Station during July 7-24, 1998. Approximately 52 miles of profiling data were collected during the survey from areas northwest of the Air Station to Flanner Beach and southeast to Cherry Point. Positioning of the seismic lines was done by using an integrated navigational system.\r\n\r\nData from the survey were used to define and delineate paleochannel alignments under the Neuse River near the Air Station. These data also were correlated with existing surface and borehole geophysical data, including vertical seismic-profiling velocity data collected in 1995.\r\n\r\nSediments believed to be Quaternary in age were identified at varying depths on the seismic sections as undifferentiated reflectors and lack the lateral continuity of underlying reflectors believed to represent older sediments of Tertiary age. The sediments of possible Quaternary age thicken to the southeast.\r\n\r\nPaleochannels of Quaternary age and varying depths were identified beneath the Neuse River estuary. These paleochannels range in width from 870 feet to about 6,900 feet. Two zones of buried paleochannels were identified in the continuous seismic-reflection profiling data. The eastern paleochannel zone includes two large superimposed channel features identified during this study and in re-interpreted 1995 land seismic-reflection data. The second paleochannel zone, located west of the first paleochannel zone, contains several small paleochannels near the central and south shore of the Neuse River estuary between Slocum Creek and Flanner Beach. This second zone of channel features may be continuous with those mapped by the U.S. Geological Survey in 1995 using land seismic-reflection data on the southern end of the Air Station.\r\n\r\nMost of the channels were mapped at the Quaternary-Tertiary sediment boundary. These channels appear to have been cut into the older sediments and deepen in a southerly or downgradient direction. If these paleochannels continue beneath the Marine Corps Air Station and are filled with permeable sediment, they may act as conduits for ground-water flow or movement of contaminants between the surficial and underlying freshwater aquifers where confining units are breached.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994099","usgsCitation":"Cardinell, A.P., 1999, Application of continuous seismic-reflection techniques to delineate paleochannels beneath the Neuse River at U.S. Marine Corps Air Station, Cherry Point, North Carolina: U.S. Geological Survey Water-Resources Investigations Report 99-4099, iv, 29 p., https://doi.org/10.3133/wri994099.","productDescription":"iv, 29 p.","costCenters":[],"links":[{"id":394157,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_19725.htm"},{"id":158071,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4099/report-thumb.jpg"},{"id":95604,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4099/report.pdf","size":"11485","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","otherGeospatial":"Cherry Point, Neuse River at U.S. Marine Corps Air Station","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.92523956298828,\n 34.88086153393072\n ],\n [\n -76.7999267578125,\n 34.88086153393072\n ],\n [\n -76.7999267578125,\n 34.9895035675793\n ],\n [\n -76.92523956298828,\n 34.9895035675793\n ],\n [\n -76.92523956298828,\n 34.88086153393072\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac6e4b07f02db67ab24","contributors":{"authors":[{"text":"Cardinell, Alex P.","contributorId":105712,"corporation":false,"usgs":true,"family":"Cardinell","given":"Alex","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":196473,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28472,"text":"wri994104 - 1999 - Hydrogeology, water use, and simulation of flow in the High Plains aquifer in northwestern Oklahoma, southeastern Colorado, southwestern Kansas, northeastern New Mexico, and northwestern Texas","interactions":[],"lastModifiedDate":"2012-02-02T00:08:47","indexId":"wri994104","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4104","title":"Hydrogeology, water use, and simulation of flow in the High Plains aquifer in northwestern Oklahoma, southeastern Colorado, southwestern Kansas, northeastern New Mexico, and northwestern Texas","docAbstract":"The U.S. Geological Survey, in cooperation with the Oklahoma Water Resources Board, began a three-year study of the High Plains aquifer in northwestern Oklahoma in 1996. The primary purpose of this study was to develop a ground-water flow model to provide the Water Board with the information it needs to manage the quantity of water withdrawn from the aquifer. The study area consists of about 7,100 square miles in Oklahoma and about 20,800 square miles in adjacent states to provide appropriate hydrologic boundaries for the flow model.\r\n\r\nThe High Plains aquifer includes all sediments from the base of the Ogallala Formation to the potentiometric surface. The saturated thickness in Oklahoma ranges from more than 400 feet to less than 50 feet. Natural recharge to the aquifer from precipitation occurs throughout the area but is extremely variable. Dryland agricultural practices appear to enhance recharge from precipitation, and part of the water pumped for irrigation also recharges the aquifer. Natural discharge occurs as discharge to streams, evapotranspiration where the depth to water is shallow, and diffuse ground-water flow across the eastern boundary. Artificial discharge occurs as discharge to wells.\r\n\r\nIrrigation accounted for 96 percent of all use of water from the High Plains aquifer in the Oklahoma portion of the study area in 1992 and 93 percent in 1997. Total estimated water use in 1992 for the Oklahoma portion of the study area was 396,000 acre-feet and was about 3.2 million acre-feet for the entire study area.\r\n\r\nSince development of the aquifer, water levels have declined more than 100 feet in small areas of Texas County, Oklahoma, and more than 50 feet in areas of Cimarron County. Only a small area of Beaver County had declines of more than 10 feet, and Ellis County had rises of more than 10 feet.\r\n\r\nA flow model constructed using the MODFLOW computer code had 21,073 active cells in one layer and had a 6,000- foot grid in both the north-south and east-west directions. The model was used to simulate the period before major development of the aquifer and the period of development. The model was calibrated using observed conditions available as of 1998.\r\n\r\nThe predevelopment-period model integrated data or estimates on the base of aquifer, hydraulic conductivity, streambed and drain conductances, and recharge from precipitation to calculate the predevelopment altitude of the water table, discharge to the rivers and streams, and other discharges. Hydraulic conductivity, recharge, and streambed conductance were varied during calibration so that the model produced a reasonable representation of the observed water table altitude and the estimated discharge to streams. Hydraulic conductivity was reduced in the area of salt dissolution in underlying Permianage rocks. Recharge from precipitation was estimated to be 4.0 percent of precipitation in greater recharge zones and 0.37 percent in lesser recharge zones. Within Oklahoma, the mean difference between water levels simulated by the model and measured water levels at 86 observation points is -2.8 feet, the mean absolute difference is 44.1 feet, and the root mean square difference is 52.0 feet. The simulated discharge is much larger than the estimated discharge for the Beaver River, is somewhat larger for Cimarron River and Wolf Creek, and is about the same for Crooked Creek.\r\n\r\nThe development-period model added specific yield, pumpage, and recharge due to irrigation and dryland cultivation to simulate the period 1946 through 1997. During calibration, estimated specific yield was reduced by 15 percent in Oklahoma east of the Cimarron-Texas County line. Simulated recharge due to irrigation ranges from 24 percent for the 1940s and 1950s to 2 percent for the 1990s. Estimated recharge due to dryland cultivation is about 3.9 percent of precipitation. The mean difference between the simulated and observed waterlevel changes from predevelopment to 1998 at 162 observation points in","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nInformation Services [distributor],","doi":"10.3133/wri994104","usgsCitation":"Luckey, R., and Becker, M.F., 1999, Hydrogeology, water use, and simulation of flow in the High Plains aquifer in northwestern Oklahoma, southeastern Colorado, southwestern Kansas, northeastern New Mexico, and northwestern Texas: U.S. Geological Survey Water-Resources Investigations Report 99-4104, v, 68 p. :ill., maps (some col.) ;28 cm., https://doi.org/10.3133/wri994104.","productDescription":"v, 68 p. :ill., maps (some col.) ;28 cm.","costCenters":[],"links":[{"id":159130,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2315,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri994104/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2de4b07f02db61476d","contributors":{"authors":[{"text":"Luckey, Richard L.","contributorId":82359,"corporation":false,"usgs":true,"family":"Luckey","given":"Richard L.","affiliations":[],"preferred":false,"id":199862,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Becker, Mark F.","contributorId":40180,"corporation":false,"usgs":true,"family":"Becker","given":"Mark","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":199861,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25560,"text":"wri994070 - 1999 - Ground-water resources in Kaloko-Honokohau National Historical Park, Island of Hawaii, and numerical simulation of the effects of ground-water withdrawals","interactions":[],"lastModifiedDate":"2023-03-13T20:46:52.570508","indexId":"wri994070","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4070","title":"Ground-water resources in Kaloko-Honokohau National Historical Park, Island of Hawaii, and numerical simulation of the effects of ground-water withdrawals","docAbstract":"Within the Kaloko-Honokohau National Historical Park, which was established in 1978, the ground-water flow system is composed of brackish water overlying saltwater. Ground-water levels measured in the Park range from about 1 to 2 feet above mean sea level, and fluctuate daily by about 0.5 to 1.5 feet in response to ocean tides. The brackish water is formed by mixing of seaward flowing fresh ground water with underlying saltwater from the ocean. The major source of fresh ground water is from subsurface flow originating from inland areas to the east of the Park. Ground-water recharge from the direct infiltration of precipitation within the Park area, which has land-surface altitudes less than 100 feet, is small because of low rainfall and high rates of evaporation. Brackish water flowing through the Park ultimately discharges to the fishponds in the Park or to the ocean. The ground water, fishponds, and anchialine ponds in the Park are hydrologically connected; thus, the water levels in the ponds mark the local position of the water table. \r\n\r\nWithin the Park, ground water near the water table is brackish; measured chloride concentrations of water samples from three exploratory wells in the Park range from 2,610 to 5,910 milligrams per liter. Chromium and copper were detected in water samples from the three wells in the Park and one well upgradient of the Park at concentrations of 1 to 5 micrograms per liter. One semi-volatile organic compound, phenol, was detected in water samples from the three wells in the Park at concentrations between 4 and 10 micrograms per liter. \r\n\r\nA regional, two-dimensional (areal), freshwater-saltwater, sharp-interface ground-water flow model was used to simulate the effects of regional withdrawals on ground-water flow within the Park. For average 1978 withdrawal rates, the estimated rate of fresh ground-water discharge to the ocean within the Park is about 6.48 million gallons per day, or about 3 million gallons per day per mile of coastline. Although the coastal discharge within the Park is actually brackish water, the model assumes that freshwater and saltwater do not mix and therefore the model-calculated coastal discharge within the Park is in the form of freshwater discharge.\r\n\r\nModel results indicate that ground-water withdrawals in excess of average 1978 withdrawal rates will reduce the rate of freshwater coastal discharge within the Park. Withdrawals from wells directly upgradient of the Park had the greatest effect on the model-calculated freshwater coastal discharge within the Park, whereas withdrawals from wells south of Papa Bay had little effect on the freshwater discharge within the Park. For an increased ground-water withdrawal rate of 56.8 million gallons per day, relative to average 1978 withdrawal rates in the Kona area, model-calculated freshwater coastal discharge within the Park was reduced by about 47 percent.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994070","usgsCitation":"Oki, D.S., Tribble, G.W., Souza, W.R., and Bolke, E.L., 1999, Ground-water resources in Kaloko-Honokohau National Historical Park, Island of Hawaii, and numerical simulation of the effects of ground-water withdrawals: U.S. Geological Survey Water-Resources Investigations Report 99-4070, vi, 49 p., https://doi.org/10.3133/wri994070.","productDescription":"vi, 49 p.","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":157732,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4070/report-thumb.jpg"},{"id":95537,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4070/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":414047,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_23011.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Kaloko-Honokohau National Historical Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.05,\n 19.7\n ],\n [\n -156.05,\n 19.667\n ],\n [\n -156.017,\n 19.667\n ],\n [\n -156.017,\n 19.7\n ],\n [\n -156.05,\n 19.7\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b01e4b07f02db6986e2","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":194194,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tribble, Gordon W. gtribble@usgs.gov","contributorId":2643,"corporation":false,"usgs":true,"family":"Tribble","given":"Gordon","email":"gtribble@usgs.gov","middleInitial":"W.","affiliations":[],"preferred":true,"id":194195,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Souza, William R.","contributorId":90295,"corporation":false,"usgs":true,"family":"Souza","given":"William","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":194197,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bolke, Edward L.","contributorId":44957,"corporation":false,"usgs":true,"family":"Bolke","given":"Edward","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":194196,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":28029,"text":"wri994080 - 1999 - Environmental setting and water-quality issues in the lower Tennessee River basin","interactions":[],"lastModifiedDate":"2012-02-02T00:08:25","indexId":"wri994080","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4080","title":"Environmental setting and water-quality issues in the lower Tennessee River basin","docAbstract":"The goals of the National Water-Quality Assessment Program are to describe current water-quality conditions for a large part of the Nation's water resources, identify water-quality changes over time, and identify the primary natural and human factors that affect water quality. The lower Tennessee River Basin is one of 59 river basins selected for study. The water-quality assessment of the lower Tennessee River Basin study unit began in 1997. The lower Tennessee River Basin study unit encompasses an area of about 19,500 square miles and extends from Chattanooga, Tennessee, to Paducah, Kentucky. The study unit had a population of about 1.5 million people in 1995.The study unit was subdivided into subunits with relatively homogeneous geology and physiography. Subdivision of the study unit creates a framework to assess the effects of natural and cultural settings on water quality. Nine subunits were delineated in the study unit; their boundaries generally coincide with level III and level IV ecoregion boundaries. The nine subunits are the Coastal Plain, Transition, Western Highland Rim, Outer Nashville Basin, Inner Nashville Basin, Eastern Highland Rim, Plateau Escarpment and Valleys, Cumberland Plateau, and Valley and Ridge.The lower Tennessee River Basin consists of predominantly forest (51 percent) and agricultural land (40 percent). Activities related to agricultural land use, therefore, are the primary cultural factors likely to have a widespread effect on surface- and ground-water quality in the study unit. Inputs of total nitrogen and phosphorus from agricultural activities in 1992 were about 161,000 and 37,900 tons, respectively. About 3.7 million pounds (active ingredient) of pesticides was applied to crops in the lower Tennessee River Basin in 1992.State water-quality agencies identified nutrient enrichment and pathogens as water-quality issues affecting both surface and ground water in the lower Tennessee River Basin. Water-quality data collected by State and Federal agencies between 1980 and 1996 were summarized to characterize surface- and ground-water quality of the subunits with respect to these issues. Median concentrations of nitrogen species generally were less than 1 milligram per liter in surface and ground water in all subunits, and were highest throughout the subunits that had the largest percentages of agricultural land use. Median phosphorus concentrations also were less than 1 milligram per liter in all subunits. Phosphatic limestones present in two subunits had a larger effect on phosphorus concentrations in surface and ground water than did the amount of agricultural land use in these subunits. Median counts of fecal coliform were higher in surface water than in ground water in all subunits. The highest median counts in surface water were in the Valley and Ridge (7,500 colonies per 100 milliliters) and the Outer Nashville Basin subunits (5,000 colonies per 100 milliliters). Highest median counts in ground water were in the Inner and Outer Nashville Basin subunit. Natural setting likely has an important effect with respect to fecal contamination of surface and ground water in the lower Tennessee River Basin.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri994080","usgsCitation":"Kingsbury, J.A., Hoos, A.B., and Woodside, M.D., 1999, Environmental setting and water-quality issues in the lower Tennessee River basin: U.S. Geological Survey Water-Resources Investigations Report 99-4080, vii, 44 p. :ill. (some col.), col. maps ;28 cm., https://doi.org/10.3133/wri994080.","productDescription":"vii, 44 p. :ill. (some col.), col. maps ;28 cm.","costCenters":[],"links":[{"id":157642,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2118,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri994080","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a13e4b07f02db602187","contributors":{"authors":[{"text":"Kingsbury, James A. 0000-0003-4985-275X jakingsb@usgs.gov","orcid":"https://orcid.org/0000-0003-4985-275X","contributorId":883,"corporation":false,"usgs":true,"family":"Kingsbury","given":"James","email":"jakingsb@usgs.gov","middleInitial":"A.","affiliations":[{"id":24708,"text":"Lower Mississippi-Gulf Water Science Center","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true},{"id":581,"text":"Tennessee Water Science Center","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"preferred":true,"id":199093,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hoos, Anne B. abhoos@usgs.gov","contributorId":2236,"corporation":false,"usgs":true,"family":"Hoos","given":"Anne","email":"abhoos@usgs.gov","middleInitial":"B.","affiliations":[],"preferred":true,"id":199094,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Woodside, M. D.","contributorId":98722,"corporation":false,"usgs":true,"family":"Woodside","given":"M.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":199095,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":27949,"text":"wri994242 - 1999 - Estimation of potential runoff-contributing areas in Kansas using topographic and soil information","interactions":[],"lastModifiedDate":"2012-02-02T00:08:40","indexId":"wri994242","displayToPublicDate":"2001-03-01T00:00:00","publicationYear":"1999","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":"99-4242","title":"Estimation of potential runoff-contributing areas in Kansas using topographic and soil information","docAbstract":"Digital topographic and soil information was used to estimate potential runoff-contributing areas throughout Kansas. The results then were used to compare 91 selected subbasins representing soil, slope, and runoff variability. Potential runoff-contributing areas were estimated collectively for the processes of infiltration-excess and saturation-excess overland flow using a set of environmental conditions that represented very high, high, moderate, low, very low, and extremely low potential runoff. For infiltration-excess overland flow, various rainfall-intensity and soil-permeability values were used. For saturation-excess overland flow, antecedent soil-moisture conditions and a topographic wetness index were used. Results indicated that very low potential-runoff conditions provided the best ability to distinguish the 91 selected subbasins as having relatively high or low potential runoff. The majority of the subbasins with relatively high potential runoff are located in the eastern half of the State where soil permeability generally is less and precipitation typically is greater. The ability to distinguish the subbasins as having relatively high or low potential runoff was possible mostly due to the variability of soil permeability across the State.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nInformation Services [distributor],","doi":"10.3133/wri994242","usgsCitation":"Juracek, K.E., 1999, Estimation of potential runoff-contributing areas in Kansas using topographic and soil information: U.S. Geological Survey Water-Resources Investigations Report 99-4242, iv, 29 p. :ill., maps (some col.) ;28 cm., https://doi.org/10.3133/wri994242.","productDescription":"iv, 29 p. :ill., maps (some col.) ;28 cm.","costCenters":[],"links":[{"id":2201,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri99-4242","linkFileType":{"id":5,"text":"html"}},{"id":95690,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4242/report.pdf","size":"8783","linkFileType":{"id":1,"text":"pdf"}},{"id":158757,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4242/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ae4b07f02db5fb26f","contributors":{"authors":[{"text":"Juracek, Kyle E. 0000-0002-2102-8980 kjuracek@usgs.gov","orcid":"https://orcid.org/0000-0002-2102-8980","contributorId":2022,"corporation":false,"usgs":true,"family":"Juracek","given":"Kyle","email":"kjuracek@usgs.gov","middleInitial":"E.","affiliations":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"preferred":true,"id":198953,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":25581,"text":"wri984202 - 1999 - Hydrogeology of the upper Floridan Aquifer in the vicinity of the Marine Corps Logistics Base near Albany, Georgia","interactions":[],"lastModifiedDate":"2017-01-31T10:13:40","indexId":"wri984202","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"98-4202","title":"Hydrogeology of the upper Floridan Aquifer in the vicinity of the Marine Corps Logistics Base near Albany, Georgia","docAbstract":"In 1995, the U.S. Navy requested that the U.S. Geological Survey conduct an investigation to describe the hydrogeology of the Upper Floridan aquifer in the vicinity of the Marine Corps Logistics Base, southeast and adjacent to Albany, Georgia. The study area encompasses about 90 square miles in the Dougherty Plain District of the Coastal Plain physiographic province, in Dougherty and Worth Counties-the Marine Corps Logistics Base encompasses about 3,600 acres in the central part of the study area.\r\n\r\nThe Upper Floridan aquifer is the shallowest, most widely used source of drinking water for domestic use in the Albany area. The hydrogeologic framework of this aquifer was delineated by description of the geologic and hydrogeologic units that compose the aquifer; evaluation of the lithologic and hydrologic heterogeneity of the aquifer; comparison of the geologic and hydrogeologic setting beneath the base with those of the surrounding area; and determination of ground-water-flow directions, and vertical hydraulic conductivities and gradients in the aquifer.\r\n\r\nThe Upper Floridan aquifer is composed of the Suwannee Limestone and Ocala Limestone and is divided into an upper and lower water-bearing zone. The aquifer is confined below by the Lisbon Formation and is semi-confined above by a low-permeability clay layer in the undifferentiated overburden. The thickness of the aquifer ranges from about 165 feet in the northeastern part of the study area, to about 325 feet in the southeastern part of the study area. Based on slug tests conducted by a U.S. Navy contractor, the upper water-bearing zone has low horizontal hydraulic conductivity (0.0224 to 2.07 feet per day) and a low vertical hydraulic conductivity (0.0000227 to 0.510 feet per day); the lower water-bearing zone has a horizontal hydraulic conductivity that ranges from 0.0134 to 2.95 feet per day.\r\n\r\nWater-level hydrographs of continuously monitored wells on the Marine Corps Logistics Base show excellent correlation between ground-water level and stage of the Flint River. Ground-water-flow direction in the southwestern part of the base generally is southeast to northwest; whereas, in the northeastern part of the base, flow directions generally are east to west, as well as from west to east, thus creating a ground-water low. Ground-water flow in the larger study area generally is east to west towards the Flint River, with a major ground-water-flow path existing from the Pelham Escarpment to the Flint River and a seasonal cone of depression the size of which is dependent upon the magnitude of irrigation pumping during the summer months.\r\n\r\nCalculated vertical hydraulic gradients (based upon data from 11 well-cluster sites on the Marine Corps Logistics Base) range from 0.0016 to 0.1770 foot per foot, and generally are highest in the central and eastern parts of the base. The vertical gradient is downward at all well-cluster sites. \r\n","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, U.S. Geological Survey ;\r\nInformation Services [distributor],","doi":"10.3133/wri984202","usgsCitation":"McSwain, K.B., 1999, Hydrogeology of the upper Floridan Aquifer in the vicinity of the Marine Corps Logistics Base near Albany, Georgia: U.S. Geological Survey Water-Resources Investigations Report 98-4202, v, 49 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri984202.","productDescription":"v, 49 p. :ill., maps ;28 cm.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":157202,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1998/4202/report-thumb.jpg"},{"id":95542,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1998/4202/report.pdf","size":"7883","linkFileType":{"id":1,"text":"pdf"}},{"id":13473,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wrir98-4202/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Georgia","city":"Albany","otherGeospatial":"Marine Corps Logistics Base, Upper Floridan Aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -84.30496215820312,\n 31.21045241900757\n ],\n [\n -84.30496215820312,\n 31.668577131274454\n ],\n [\n -83.583984375,\n 31.668577131274454\n ],\n [\n -83.583984375,\n 31.21045241900757\n ],\n [\n -84.30496215820312,\n 31.21045241900757\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad7e4b07f02db6844a4","contributors":{"authors":[{"text":"McSwain, Kristen Bukowski kmcswain@usgs.gov","contributorId":1606,"corporation":false,"usgs":true,"family":"McSwain","given":"Kristen","email":"kmcswain@usgs.gov","middleInitial":"Bukowski","affiliations":[{"id":476,"text":"North Carolina Water Science Center","active":true,"usgs":true}],"preferred":false,"id":194280,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28936,"text":"wri994073 - 1999 - Geohydrology and numerical simulation of the ground-water flow system of Kona, Island of Hawaii","interactions":[],"lastModifiedDate":"2020-09-26T15:47:59.897503","indexId":"wri994073","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"99-4073","displayTitle":"Geohydrology and Numerical Simulation of the Ground-Water Flow System of Kona, Island of Hawaii","title":"Geohydrology and numerical simulation of the ground-water flow system of Kona, Island of Hawaii","docAbstract":"Prior to the early 1990's, ground-water in the Kona area, which is in the western part of the island of Hawaii, was withdrawn from wells located within about 3 mi from the coast where water levels were less than 10 feet above sea level. In 1990, exploratory drilling in the uplands east of the existing coastal wells first revealed the presence of high water levels (greater than 40 feet above sea level) in the Kona area. Measured water levels from 16 wells indicate that high water levels exist in a zone parallel to and inland of the Kona coast, between Kalaoa and Honaunau. Available hydrologic and geophysical evidence is generally consistent with the concept that the high ground-water levels are associated with a buried dike complex. \r\n\r\nA two-dimensional (areal), steady-state, freshwater-saltwater, sharp-interface ground-water flow model was developed for the Kona area of the island of Hawaii, to enhance the understanding of (1) the distribution of aquifer hydraulic properties, (2) the conceptual framework of the ground-water flow system, and (3) the regional effects of ground-water withdrawals on water levels and coastal discharge. The model uses the finite-difference code SHARP. \r\n\r\nTo estimate the hydraulic characteristics, average recharge, withdrawals, and water-level conditions for the period 1991-93 were simulated. The following horizontal hydraulic-conductivity values were estimated: (1) 7,500 feet per day for the dike-free volcanic rocks of Hualalai and Mauna Loa, (2) 0.1 feet per day for the buried dike complex of Hualalai, (3) 10 feet per day for the northern marginal dike zone (north of Kalaoa), and (4) 0.5 feet per day for the southern marginal dike zone between Palani Junction and Holualoa. The coastal leakance was estimated to be 0.05 feet per day per foot. \r\n\r\nMeasured water levels indicate that ground water generally flows from inland areas to the coast. Model results are in general agreement with the limited set of measured water levels in the Kona area. Model results indicate, however, that water levels do not strictly increase in an inland direction and that a ground-water divide exists within the buried dike complex. Data are not available, however, to verify model results in the area near and inland of the model-calculated ground-water divide. \r\n\r\nThree simulations to determine the effects of proposed withdrawals from the high water-level area on coastal discharge and water levels, relative to model-calculated, steady-state coastal discharge and water levels for 1997 withdrawal rates, show that the effects are widespread. During 1997, the total withdrawal of ground water from the high water-level area between Palani Junction and Holualoa was about 1 million gallons per day. Model results indicate that it may not be possible to withdraw 25.6 million gallons per day of freshwater from this area between Palani Junction and Holualoa, but that it may be possible to withdraw between 5 to 8 million gallons per day from the same area. For a proposed withdrawal rate of 5.0 million gallons per day uniformly distributed to 12 sites between Palani Junction and Holualoa, the model-calculated drawdown of 0.01 foot or more extends about 9 miles north-northwest and about 7 miles south of the proposed well sites. In all scenarios, freshwater coastal discharge is reduced by an amount equal to the additional freshwater withdrawal. \r\n\r\nAdditional data needed to improve the understanding of the ground-water flow system in the Kona area include: (1) a wider spatial distribution and longer temporal distribution of water levels, (2) improved information about the subsurface geology, (3) independent estimates of hydraulic conductivity, (4) improved recharge estimates, and (5) information about the vertical distribution of salinity in ground water.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994073","usgsCitation":"Oki, D.S., 1999, Geohydrology and numerical simulation of the ground-water flow system of Kona, Island of Hawaii: U.S. Geological Survey Water-Resources Investigations Report 99-4073, vi, 70 p., https://doi.org/10.3133/wri994073.","productDescription":"vi, 70 p.","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":159151,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1999/4073/report-thumb.jpg"},{"id":95732,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4073/report.pdf","size":"9541","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Hawaii","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -156.258544921875,\n 18.79191774423444\n ],\n [\n -154.632568359375,\n 18.79191774423444\n ],\n [\n -154.632568359375,\n 20.427012814257385\n ],\n [\n -156.258544921875,\n 20.427012814257385\n ],\n [\n -156.258544921875,\n 18.79191774423444\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8da8","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":200646,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":29543,"text":"wri984224 - 1999 - Ground-water quality in the eastern part of the Silurian-Devonian and upper Carbonate aquifers in the eastern Iowa basins, Iowa and Minnesota, 1996","interactions":[],"lastModifiedDate":"2016-03-28T15:06:59","indexId":"wri984224","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"98-4224","title":"Ground-water quality in the eastern part of the Silurian-Devonian and upper Carbonate aquifers in the eastern Iowa basins, Iowa and Minnesota, 1996","docAbstract":"Ground-water samples were collected from 33 domestic wells to assess the water quality of the eastern part of the Silurian-Devonian and Upper Carbonate aquifers in the Eastern Iowa Basins National Water-Quality Assessment Program study unit. Samples were collected during June and July 1996 and analyzed for major ions, nutrients, pesticides and pesticide metabolites, volatile organic compounds, tritium, radon222, and environmental isotopes.
\nCalcium, magnesium, and bicarbonate were the dominant ions in most samples and were likely derived from the solution of carbonate minerals (calcite and dolomite) present in the aquifer materials. The dominance of sulfate in samples from several wells suggests the dissolution of evaporite minerals. Ammonia and orthophosphorus were the most commonly detected nutrients. Nitrate was detected in about half of the samples and exceeded the U.S. Environmental Protection Agency maximum contaminant level (10 milligrams per liter) in 6 percent of samples. Atrazine and metolachlor were the only pesticides detected and were present in 18 percent and 12 percent of samples, respectively. Alachlor ethanesulfonic acid and deethylatrazine were the most commonly detected pesticide metabolites and were present in 16 percent and 9 percent of samples, respectively. Radon-222 was detected in all samples, and 47 percent had concentrations in excess of the U.S. Environmental Protection Agency previously proposed maximum contaminant level (300 picocuries per liter). Radon-222 concentrations were significantly higher in samples from wells that produced recently recharged water. This relation suggests that uranium-bearing glacial deposits (Schumann, 1993) may be a source of radon-222 in the underlying aquifers.
\nThe presence of regional confining units and thick overlying Quaternary-age deposits have an effect on water quality in the Silurian-Devonian and Upper Carbonate aquifers in the study area. Tritium-based ground-water ages were significantly older, and dissolved-solids concentrations were significantly higher in relatively well protected areas (where the aquifers are overlain by a bedrock confining unit or more than 100 feet of Quaternary-age deposits). Ammonia concentrations were significantly higher in relatively well protected areas and in samples from wells that produced older water. Higher ammonia concentrations also were observed in ground water with dissolved-oxygen concentrations of 0.5 milligram per liter or less, allowing for the anaerobic reduction of nitrate to ammonia. Nitrate concentrations were significantly higher in relatively poorly protected areas (where the aquifers are not overlain by a bedrock confining unit or are overlain by less than 100 feet of Quaternaryage deposits) and in samples from wells that produced recently recharged water. Pesticide and metabolite concentrations were significantly higher in samples from wells that produced recently recharged water. Atrazine, metolachlor, and deethylatrazine were not detected in any samples from relatively well protected areas of the aquifers.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Iowa City, IA","doi":"10.3133/wri984224","usgsCitation":"Savoca, M.E., Sadorf, E.M., and Akers, K.K., 1999, Ground-water quality in the eastern part of the Silurian-Devonian and upper Carbonate aquifers in the eastern Iowa basins, Iowa and Minnesota, 1996: U.S. Geological Survey Water-Resources Investigations Report 98-4224, vi, 31 p., https://doi.org/10.3133/wri984224.","productDescription":"vi, 31 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":159802,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2382,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/1998/wri984224/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Iowa, Minnesota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.614990234375,\n 40.91351257612758\n ],\n [\n -91.3623046875,\n 40.83874913796459\n ],\n [\n -91.07666015625,\n 40.72228267283148\n ],\n [\n -91.20849609375,\n 40.9052096972736\n ],\n [\n -91.29638671875,\n 41.03793062246529\n ],\n [\n -91.16455078125,\n 41.1455697310095\n ],\n [\n -91.087646484375,\n 41.15384235711447\n ],\n [\n -91.175537109375,\n 41.261291493919856\n ],\n [\n -91.07666015625,\n 41.393294288784865\n ],\n [\n -91.065673828125,\n 41.52502957323801\n ],\n [\n -90.8349609375,\n 41.590796851056005\n ],\n [\n -90.615234375,\n 41.6154423246811\n ],\n [\n -90.3955078125,\n 41.68932225997044\n ],\n [\n -90.28564453124999,\n 41.83682786072714\n ],\n [\n -90.406494140625,\n 41.983994270935625\n ],\n [\n -90.670166015625,\n 41.983994270935625\n ],\n [\n -90.966796875,\n 42.06560675405716\n ],\n [\n -91.38427734374999,\n 42.24478535602799\n ],\n [\n -91.58203125,\n 42.431565872579185\n ],\n [\n -91.92260742187499,\n 42.706659563510385\n ],\n [\n -92.208251953125,\n 42.94838139765314\n ],\n [\n -92.48291015625,\n 43.17313537107136\n ],\n [\n -92.6806640625,\n 43.42898792344157\n ],\n [\n -92.92236328125,\n 43.723474896114816\n ],\n [\n -93.065185546875,\n 43.94537239244209\n ],\n [\n -93.262939453125,\n 44.07969327425713\n ],\n [\n -93.460693359375,\n 44.01652134387754\n ],\n [\n -93.61450195312499,\n 43.937461690316646\n ],\n [\n -93.84521484375,\n 43.76315996157264\n ],\n [\n -93.9990234375,\n 43.48481212891603\n ],\n [\n -94.10888671875,\n 43.34116005412307\n ],\n [\n -94.163818359375,\n 43.1811470593997\n ],\n [\n -94.075927734375,\n 43.08493742707592\n ],\n [\n -93.93310546875,\n 42.956422511073335\n ],\n [\n -93.834228515625,\n 42.779275360241904\n ],\n [\n -93.84521484375,\n 42.577354839557856\n ],\n [\n -94.010009765625,\n 42.44778143462245\n ],\n [\n -94.06494140625,\n 42.26917949243506\n ],\n [\n -94.04296874999999,\n 42.00848901572399\n ],\n [\n -93.878173828125,\n 41.77131167976407\n ],\n [\n -93.53759765625,\n 41.50857729743935\n ],\n [\n -93.05419921875,\n 41.45919537950706\n ],\n [\n -92.757568359375,\n 41.261291493919856\n ],\n [\n -92.427978515625,\n 41.12074559016745\n ],\n [\n -92.17529296875,\n 41.0130657870063\n ],\n [\n -91.812744140625,\n 40.94671366508002\n ],\n [\n -91.614990234375,\n 40.91351257612758\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db6671c5","contributors":{"authors":[{"text":"Savoca, Mark E. mesavoca@usgs.gov","contributorId":1961,"corporation":false,"usgs":true,"family":"Savoca","given":"Mark","email":"mesavoca@usgs.gov","middleInitial":"E.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"preferred":true,"id":201690,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sadorf, Eric M. emsadorf@usgs.gov","contributorId":2245,"corporation":false,"usgs":true,"family":"Sadorf","given":"Eric","email":"emsadorf@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":201691,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Akers, Kymm K.B.","contributorId":20790,"corporation":false,"usgs":true,"family":"Akers","given":"Kymm","email":"","middleInitial":"K.B.","affiliations":[],"preferred":false,"id":201692,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":27600,"text":"wri994075 - 1999 - The Sparta aquifer in Arkansas' critical ground-water areas: Response of the aquifer to supplying future water needs","interactions":[],"lastModifiedDate":"2015-10-22T13:19:40","indexId":"wri994075","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"99-4075","title":"The Sparta aquifer in Arkansas' critical ground-water areas: Response of the aquifer to supplying future water needs","docAbstract":"The Sparta aquifer is a confined aquifer of great regional importance that comprises a sequence of unconsolidated sand, silt, and clay units extending across much of eastern and southeastern Arkansas and into adjoining States. Water use from the aquifer has doubled since 1975 and continues to increase, and large water-level declines are occurring in many areas of the aquifer. To focus State attention and resources on the growing problem and to provide a mechanism for locally based education and management, the Arkansas Soil and Water Conservation Commission has designated Critical Ground-Water Areas in some counties (see page 6, ?What is a Critical Ground-Water Area??). Ground-water modeling study results show that the aquifer cannot continue to meet growing water-use demands. Dewatering of the primary producing sands is predicted to occur within 10 years in some areas if current trends continue. The predicted dewatering will cause reduced yields and damage the aquifer. Modeling also shows that a concerted ground-water conservation management plan could enable sustainable use of the aquifer. Water-conservation measures and use of alternative sources that water managers in Union County (an area of high demand and growth in Arkansas' initial five-county Critical Ground-Water Area) think to be realistic options result in considerable recovery in water levels in the aquifer during a 30-year model simulation.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994075","usgsCitation":"Hays, P.D., and Fugitt, D.T., 1999, The Sparta aquifer in Arkansas' critical ground-water areas: Response of the aquifer to supplying future water needs: U.S. Geological Survey Water-Resources Investigations Report 99-4075, 5 p., https://doi.org/10.3133/wri994075.","productDescription":"5 p.","numberOfPages":"5","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":310509,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1999/4075/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}},{"id":158873,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri994075.jpg"}],"country":"United States","state":"Arkansas","otherGeospatial":"Sparta Aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -94.3505859375,\n 33.742612777346885\n ],\n [\n -91.73583984374999,\n 36.527294814546245\n ],\n [\n -89.93408203124999,\n 36.527294814546245\n ],\n [\n -89.69238281249999,\n 36.13787471840729\n ],\n [\n -90.28564453124999,\n 34.95799531086792\n ],\n [\n -90.90087890624999,\n 34.10725639663118\n ],\n [\n -91.20849609375,\n 33.33970700424026\n ],\n [\n -91.23046875,\n 32.99023555965106\n ],\n [\n -93.0322265625,\n 32.99023555965106\n ],\n [\n -94.06494140625,\n 33.02708758002874\n ],\n [\n -94.3505859375,\n 33.742612777346885\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac6e4b07f02db67a902","contributors":{"authors":[{"text":"Hays, Phillip D. 0000-0001-5491-9272 pdhays@usgs.gov","orcid":"https://orcid.org/0000-0001-5491-9272","contributorId":4145,"corporation":false,"usgs":true,"family":"Hays","given":"Phillip","email":"pdhays@usgs.gov","middleInitial":"D.","affiliations":[{"id":24708,"text":"Lower Mississippi-Gulf Water Science Center","active":true,"usgs":true},{"id":369,"text":"Louisiana Water Science Center","active":true,"usgs":true},{"id":129,"text":"Arkansas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":198393,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fugitt, D. Todd","contributorId":7835,"corporation":false,"usgs":true,"family":"Fugitt","given":"D.","email":"","middleInitial":"Todd","affiliations":[],"preferred":false,"id":198394,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":25746,"text":"wri994162 - 1999 - Relation of arsenic, iron, and manganese in ground water to aquifer type, bedrock lithogeochemistry, and land use in the New England coastal basins","interactions":[],"lastModifiedDate":"2023-04-03T21:26:49.37968","indexId":"wri994162","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"99-4162","title":"Relation of arsenic, iron, and manganese in ground water to aquifer type, bedrock lithogeochemistry, and land use in the New England coastal basins","docAbstract":"In a study of arsenic concentrations in public-supply wells in the New England Coastal Basins, concentrations at or above 0.005 mg/L (milligrams per liter) were detected in more samples of water from wells completed in bedrock (25 percent of all samples) than in water from wells completed in stratified drift (7.5 percent of all samples). Iron and manganese were detected (at concentrations of 0.05 and 0.03 mg/L, respectively) at approximately the same frequency in water from wells in both types of aquifers.
Concentrations of arsenic in public-supply wells drilled in bedrock (in the National Water-Quality Assessment Program New England Coastal Basins study unit) vary with the bedrock lithology. Broad groups of lithogeochemical units generalized from bedrock lithologic units shown on state geologic maps were used in the statistical analyses. Concentrations of arsenic in water from public-supply wells in metasedimentary bedrock units that contain slightly to moderately calcareous and calcsilicate rocks (lithogeochemical group Mc) were significantly higher than the concentrations in five other groups of bedrock units in the study unit. Arsenic was detected, at or above 0.005 mg/L, in water from 44 percent of the wells in the lithogeochemical group M c and in water from less than 28 percent of wells in the five other groups. Additionally, arsenic concentrations in ground water were the lowest in the metasedimentary rocks that are characterized as variably sulfidic (group Ms ). Generally, concentrations of arsenic were low in water from bedrock wells in the felsic igneous rocks (group If ) though locally some bedrock wells in granitic rocks are known to have ground water with high arsenic concentrations, especially in New Hampshire.
The concentrations of arsenic in ground water also correlate with land-use data; significantly higher concentrations are found in areas identified as agricultural land use than in undeveloped areas. There is, however, more agricultural land in areas overlying the metasedimentary rocks of lithogeochemical groups Mc and the minimally-deformed clastic sediments of group Mmd than in areas overlying other lithogeochemical groups. This correlation complicates the interpretation of sources of arsenic to ground water in bedrock. A test of this association revealed that relations between arsenic concentrations and the metasedimentary rocks of group Mc are not weakened when data associated with agricultural land use is removed; the reverse is true, however, if the data associated with the group Mc are removed from the analysis.
The occurrence and variability of arsenic in water from bedrock supply wells could be related to several factors. These include (1) the distribution and chemical form of arsenic in soils and rocks that are part of the ground-water-flow system, (2) the characteristics that influence the solubility and transport of arsenic in ground water, (3) the differing degrees of vulnerability of ground-water supplies to surface contamination, and (4) the spatial associations between land use, geology, and ground-water-flow patterns. Strong relations between agricultural land use and the metasedimentary rocks of group Mc complicate the interpretation of arsenic source to water in these bedrock aquifers. This is due in part to the past use of arsenical pesticides; additionally, few whole-rock geochemical data are available for the rock types in the lithogeochemical groups of aquifers that contain ground water with elevated concentrations of arsenic. Without such data, identifying specific bedrock types as arsenic sources is not possible. In southern Maine and south-central New Hampshire, and in northern Massachusetts, the few available whole-rock analyses suggest, at least for these local areas, a connection between known bedrock chemistry and ground-water arsenic levels.
Although the lithogeochemical group and land-use category variables individually describe much of the variance in the concentrations of arsenic in ground water, the lithogeochemical relation is statistically stronger than the land-use relation. Low concentrations of arsenic in water from bedrock public-supply wells are associated with the metasedimentary rocks of group Ms (characterized as variably sulfidic). This association could reflect a variety of factors and suggests that simple dissolution of arsenic-bearing iron phases, such as sulfides, may not explain concentrations of arsenic in water in this bedrock aquifer group. Whole-rock geochemical data and more complete water-chemistry data, as well as studies of historical variation of arsenic concentrations (time-line studies), and site-specific studies, will be critical in addressing the arsenic source issue.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri994162","usgsCitation":"Ayotte, J., Nielsen, M.G., Robinson, G.R., and Moore, R.B., 1999, Relation of arsenic, iron, and manganese in ground water to aquifer type, bedrock lithogeochemistry, and land use in the New England coastal basins: U.S. Geological Survey Water-Resources Investigations Report 99-4162, v, 63 p., https://doi.org/10.3133/wri994162.","productDescription":"v, 63 p.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":371,"text":"Maine Water Science Center","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"links":[{"id":156171,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":415127,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_22932.htm","linkFileType":{"id":5,"text":"html"}},{"id":1865,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri994162","linkFileType":{"id":5,"text":"html"}}],"country":"United States","otherGeospatial":"New England coastal basins","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -69.083,\n 46\n ],\n [\n -72,\n 46\n ],\n [\n -72,\n 41.3\n ],\n [\n -69.083,\n 41.3\n ],\n [\n -69.083,\n 46\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c303","contributors":{"authors":[{"text":"Ayotte, Joseph D. jayotte@usgs.gov","contributorId":1802,"corporation":false,"usgs":true,"family":"Ayotte","given":"Joseph D.","email":"jayotte@usgs.gov","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":false,"id":194900,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nielsen, Martha G. 0000-0003-3038-9400 mnielsen@usgs.gov","orcid":"https://orcid.org/0000-0003-3038-9400","contributorId":4169,"corporation":false,"usgs":true,"family":"Nielsen","given":"Martha","email":"mnielsen@usgs.gov","middleInitial":"G.","affiliations":[{"id":37947,"text":"Upper Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":194902,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Robinson, Gilpin R. Jr. grobinso@usgs.gov","contributorId":3083,"corporation":false,"usgs":true,"family":"Robinson","given":"Gilpin","suffix":"Jr.","email":"grobinso@usgs.gov","middleInitial":"R.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":false,"id":194901,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Moore, Richard B. rmoore@usgs.gov","contributorId":1464,"corporation":false,"usgs":true,"family":"Moore","given":"Richard","email":"rmoore@usgs.gov","middleInitial":"B.","affiliations":[{"id":405,"text":"NH/VT office of New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":194899,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":25790,"text":"wri994211 - 1999 - Surface-geophysical investigation of the University of Connecticut landfill, Storrs, Connecticut","interactions":[],"lastModifiedDate":"2019-10-16T06:39:19","indexId":"wri994211","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"99-4211","title":"Surface-geophysical investigation of the University of Connecticut landfill, Storrs, Connecticut","docAbstract":"A surface-geophysical investigation of the former landfill area at the University of Connecticut in Storrs, Conn. was conducted as part of a preliminary hydrogeologic assessment of the contamination of soil, surface water, and ground water at the site. Geophysical data were used to help determine the dominant direction of fracture strike; subsurface structure of the landfill; locations of possible leachate plumes, fracture zones or conductive lithologic layers; and the location and number of chemical waste-disposal pits. Azimuthal square-array direct-current (dc) resistivity, two-dimensional (2D) dc-resistivity, inductive terrain conductivity, and ground-penetrating radar (GPR) were the methods used to characterize the landfill area.The dominant strike direction of bedrock fractures interpreted from azimuthal square-array resistivity data is north, ranging from 285 to 30 degrees east of True North. These results complement local geologic maps that identify bedrock foliation and fractures that strike approximately north-south and dip 30 to 40 degrees west.The subsurface structure of the landfill was imaged with 2D dc-resistivity profiling data, which were used to interpret a landfill thickness of 10 to 15 meters. Orientation of the landfill trash disposal trenches were detected by azimuthal square-array resistivity soundings; the dimension and the orientation of the trenches were verified by aerial photographs.Inductive terrain conductivity and 2D dc-resistivity profiling detected conductive anomalies that were interpreted as possible leachate plumes near two surface-water discharge areas. The conductive anomaly to the north of the landfill is interpreted to be a shallow leachate plume and dissipates to almost background levels 45 meters north of the landfill. The anomaly to the southwest is interpreted to extend vertically through the overburden and into the shallow bedrock and laterally along the intermittent drainage to Eagleville Brook, terminating 140 meters south of the landfill. Inductive terrain conductivity and 2D dc-resistivity profiling also detected two dipping, sheet-like conductive features that extend vertically into the bedrock. These features were interpreted either as fracture zones filled with conductive fluids or conductive lithologic layers between more resistive layers. One dipping conductive feature was detected south of the landfill, and the other feature was detected to the west of the former chemical waste-disposal pits. Both anomalies strike approximately north-south and dip about 30 degrees to the west.GPR was used unsuccessfully to locate the former chemical waste-disposal pits. Although the entire overburden and the upper few meters of bedrock were imaged, no anomalous features were detected with GPR that could be correlated with the pits. It is possible that the area surveyed by GPR was entirely backfilled after the soil was removed from the site and that the outline of the former chemical waste-disposal pits no longer exists. ","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri994211","usgsCitation":"Powers, C.J., Wilson, J., Haeni, F., and Johnson, C., 1999, Surface-geophysical investigation of the University of Connecticut landfill, Storrs, Connecticut: U.S. Geological Survey Water-Resources Investigations Report 99-4211, v, 34 p., https://doi.org/10.3133/wri994211.","productDescription":"v, 34 p.","costCenters":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"links":[{"id":158352,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":2044,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://water.usgs.gov/ogw/bgas/publications/wri994211/wri994211.pdf","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Connecticut","city":"Storrs","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72.27750778198242,\n 41.81073178596062\n ],\n [\n -72.2519302368164,\n 41.81073178596062\n ],\n [\n -72.2519302368164,\n 41.821606443011916\n ],\n [\n -72.27750778198242,\n 41.821606443011916\n ],\n [\n -72.27750778198242,\n 41.81073178596062\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae5e4b07f02db68a80b","contributors":{"authors":[{"text":"Powers, Christopher J.","contributorId":41464,"corporation":false,"usgs":true,"family":"Powers","given":"Christopher","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":195085,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilson, Joanna","contributorId":58685,"corporation":false,"usgs":true,"family":"Wilson","given":"Joanna","affiliations":[],"preferred":false,"id":195086,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Haeni, F.P.","contributorId":87105,"corporation":false,"usgs":true,"family":"Haeni","given":"F.P.","affiliations":[],"preferred":false,"id":195087,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Johnson, C. D.","contributorId":8120,"corporation":false,"usgs":true,"family":"Johnson","given":"C. D.","affiliations":[],"preferred":false,"id":195084,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":30233,"text":"wri994134 - 1999 - Regional water-level changes for the Cambrian-Ordovician aquifer in Iowa, 1975 to 1997","interactions":[],"lastModifiedDate":"2022-11-23T22:24:26.309098","indexId":"wri994134","displayToPublicDate":"2001-02-01T00:00:00","publicationYear":"1999","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":"99-4134","title":"Regional water-level changes for the Cambrian-Ordovician aquifer in Iowa, 1975 to 1997","docAbstract":"The Cambrian-Ordovician aquifer is one of the principal sources of ground water for industry and municipalities in Iowa. The 1998 Iowa Administrative Code Chapter 52.4(3) states that water levels in the Cambrian-Ordovician aquifer are not to decline more than 200 feet from the 1977 baseline. The potentiometric-surface map of the Cambrian-Ordovician aquifer, known locally as the Jordan aquifer, prepared by the Iowa Department of Natural Resources-Geological Survey Bureau and the U.S. Geological Survey in 1978 using water levels measured during the 1975 water year is considered the 1977 baseline.
\nFor this study, water levels measured during the 1997 water year were used to construct a potentiometric-surface map that was compared to the 1977 baseline to describe water-level changes. Since 1975, water levels have declined in two areas of central and eastern Iowa. The maximum measured water-level decline is 133 feet in Johnson County in eastern Iowa. The estimated maximum rate of decline is 6 feet per year in Johnson County.
\nResults from a two-layer, ground-water flow model of the Cambrian-Ordovician aquifer constructed by the U.S. Geological Survey in 1990 were compared to selected measured 1997 water levels. The difference between the simulated water levels and the 1997 maximum measured water levels ranges from 0 to about 150 feet, but most differences are less than 25 feet. The comparison indicates that the model may help estimate future water levels in the Cambrian-Ordovician aquifer as an aid in managing the resource.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Iowa City, IA","doi":"10.3133/wri994134","collaboration":"Prepared in cooperation with the Iowa Department Natural Resources, Geological Survey Bureau","usgsCitation":"Turco, M.J., 1999, Regional water-level changes for the Cambrian-Ordovician aquifer in Iowa, 1975 to 1997: U.S. Geological Survey Water-Resources Investigations Report 99-4134, iv, 11 p., https://doi.org/10.3133/wri994134.","productDescription":"iv, 11 p.","numberOfPages":"18","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":409624,"rank":3,"type":{"id":36,"text":"NGMDB Index 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]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c42b","contributors":{"authors":[{"text":"Turco, Michael J. mjturco@usgs.gov","contributorId":1011,"corporation":false,"usgs":true,"family":"Turco","given":"Michael","email":"mjturco@usgs.gov","middleInitial":"J.","affiliations":[],"preferred":true,"id":202903,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30218,"text":"wri984263 - 1999 - Geohydrology of Pipe Spring National Monument area, northern Arizona","interactions":[],"lastModifiedDate":"2019-08-29T09:13:08","indexId":"wri984263","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"1999","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":"98-4263","title":"Geohydrology of Pipe Spring National Monument area, northern Arizona","docAbstract":"Pipe Spring National Monument is on the Arizona Strip, an area between the Utah border to the north and the north rim of the Grand Canyon to the south. Four springs at the base of Winsor Point on Winsor Mountain (known collectively as Pipe Spring) are a part of the historical significance of the monument. The relation between declining discharges from springs in the monument and ground-water development north of the monument was studied to provide information that could be used for management of the monument resources.\r\nGround-water elevations from wells indicate that ground-water movement is from north to south along the west side of a branch of Sevier Fault. Faulting in the areas has downthrown permeable water-bearing sediments relative to impermeable sediments and is evinced by cliffs along the western and northern edges and flat-lying areas to the east. The Navajo Sandstone and Kayenta Formation are the primary water-bearing units on the west side of the fault. The semipermeable sediments of the Chinle and Moenkopi Formations on the east side of the fault inhibit ground-water movement from the west to the east side of the fault.\r\nGround water south of Moccasin Canyon is higher in total dissolved solids than ground water north of Moccasin Canyon. Wells north of Moccasin Canyon are open primarily in the Navajo Sandstone, and wells south of Moccasin Canyon are open primarily in the upper sandstone facies of the Kayenta Formation.\r\nA water-budget estimate for the study area indicates a storage deficit of 780 acre-feet per year. This deficit suggests that some recharge may be occurring outside the study area. Oxygen and hydrogen stable- isotopic data suggest no isotopic variation in recharging waters in the study area and surrounding region. Radiocarbon and tritium activities indicate apparent ground-water ages at wells and springs are between 45 and 9,000 years.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri984263","usgsCitation":"Truini, M., 1999, Geohydrology of Pipe Spring National Monument area, northern Arizona: U.S. Geological Survey Water-Resources Investigations Report 98-4263, v, 25 p. , https://doi.org/10.3133/wri984263.","productDescription":"v, 25 p. ","costCenters":[],"links":[{"id":367050,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1998/4263/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":159300,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1998/4263/report-thumb.jpg"}],"country":"United States","state":"Arizona","otherGeospatial":"Pipe Spring National Monument","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -112.74238586425781,\n 36.8605319047265\n ],\n [\n -112.73706436157227,\n 36.8605319047265\n ],\n [\n -112.73706436157227,\n 36.86465217172221\n ],\n [\n -112.74238586425781,\n 36.86465217172221\n ],\n [\n -112.74238586425781,\n 36.8605319047265\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b28e4b07f02db6b12b9","contributors":{"authors":[{"text":"Truini, Margot mtruini@usgs.gov","contributorId":599,"corporation":false,"usgs":true,"family":"Truini","given":"Margot","email":"mtruini@usgs.gov","affiliations":[{"id":128,"text":"Arizona Water Science Center","active":true,"usgs":true}],"preferred":true,"id":202877,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":26164,"text":"wri984232 - 1999 - Streamflow, base flow, and ground-water recharge in the Housatonic River basin, western Massachusetts and parts of eastern New York and northwestern Connecticut","interactions":[],"lastModifiedDate":"2022-09-19T18:16:48.344","indexId":"wri984232","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"1999","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":"98-4232","title":"Streamflow, base flow, and ground-water recharge in the Housatonic River basin, western Massachusetts and parts of eastern New York and northwestern Connecticut","docAbstract":"Streamflows for selected flow durations from 1 to 99 percent and the August median streamflows were estimated for 11 long-term streamflow-gaging stations in and near the study area. Estimates of streamflow and associated standard errors were determined for selected flow durations from 50 to 99 percent and the August median streamflows for 21 low-flow partial-record stations and for selected flow durations from 1 to 99 percent and the August median streamflows for two partial-record stations and seven short-term discontinued streamflow-gaging stations. Median streamflows per square mile for the 10-, 50-, and 90-percent flow durations and the August median streamflows were 3.90, 1.01, 0.185, and 0.248 cubic feet per second per square mile. Streamflows per square mile at selected flow-duration discharges between 1 and 99 percent at the 41 stations were related to basin characteristics to explain differences in streamflow characteristics. Basin characteristics included basin elevations, extent of stratified-drift deposits, land use, aspect, and underlying bedrock geology types. Most streamflow differences were positively correlated to basin elevation differences, most likely because precipitation increases with elevation, and to stratified-drift deposits, which allow more precipitation to recharge the ground water and to discharge later than do till and bedrock deposits.Mean base flow was computed from continuous records of daily mean discharge at 11 long-term streamflow-gaging stations in and near the study area. Mean annual base flow ranged from 13.4 to 24.5 inches per year. Minimum annual base flow ranged from 45 to 72 percent of mean annual rates at the 11 long-term stations, and the ratio of base flow to streamflow (base-flow index) ranged from 0.55 to 0.80. Base-flow durations between 1 and 99 percent were calculated from streamflow records at the 11 long-term streamflow-gaging stations. Base flow accounted for 45.5 to 85.0 percent of total annual streamflow at the 1- and 99-percent flow durations. Ground-water-recharge rates were computed from continuous records of daily mean discharge at 11 long-term streamflow-gaging stations in and near the study area. Mean annual ground-water-recharge rates ranged from 17.5 to 22.4 inches per year at 10 of the 11 long-term stations. Mean annual ground-water-recharge rates ranged from 2 to 7 inches per year higher than base flow. Minimum annual ground-water-recharge rates ranged from 48 to 72 percent of mean annual ground-water-recharge rates. Mean annual potential ground-water recharge was estimated from monthly climatological data collected at six climatological stations in and near the study area. Mean potential ground-water recharge ranged from about 17.9 to 28.9 inches per year, with a median value of 22.6 inches per year. This median value compares well to that calculated by use of streamflow records at the 11 streamflow-gaging stations (20.0 inches per year).Streamflows per square mile for the 10-, 50-, and 90-percent flow durations at stations in and near the study area were similar to those computed for other unregulated long-term continuous streamflow-gaging stations in central and eastern Massachusetts. Base-flow and ground-water-recharge rates in the study area compared closely to results from other studies in southeastern Massachusetts and Rhode Island, which were based on the same computational methods.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri984232","usgsCitation":"Bent, G.C., 1999, Streamflow, base flow, and ground-water recharge in the Housatonic River basin, western Massachusetts and parts of eastern New York and northwestern Connecticut: U.S. Geological Survey Water-Resources Investigations Report 98-4232, v, 68 p., https://doi.org/10.3133/wri984232.","productDescription":"v, 68 p.","costCenters":[],"links":[{"id":125126,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_98_4232.jpg"},{"id":406989,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_19411.htm","linkFileType":{"id":5,"text":"html"}},{"id":2084,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri984232","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Connecticut, Massachusetts, New York","otherGeospatial":"Housatonic River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.529,\n 42\n ],\n [\n -73.033,\n 42\n ],\n [\n -73.033,\n 42.6\n ],\n [\n -73.529,\n 42.6\n ],\n [\n -73.529,\n 42\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b1e4b07f02db53056d","contributors":{"authors":[{"text":"Bent, Gardner C. 0000-0002-5085-3146 gbent@usgs.gov","orcid":"https://orcid.org/0000-0002-5085-3146","contributorId":1864,"corporation":false,"usgs":true,"family":"Bent","given":"Gardner","email":"gbent@usgs.gov","middleInitial":"C.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195924,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":28401,"text":"wri994129 - 1999 - Characteristics of water-quality data for Lake Houston, selected tributary inflows to Lake Houston, and the Trinity River near Lake Houston (a potential source of interbasin transfer), August 1983-September 1990","interactions":[],"lastModifiedDate":"2024-03-05T21:29:46.399655","indexId":"wri994129","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"1999","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":"99-4129","title":"Characteristics of water-quality data for Lake Houston, selected tributary inflows to Lake Houston, and the Trinity River near Lake Houston (a potential source of interbasin transfer), August 1983-September 1990","docAbstract":"Lake Houston, a reservoir completed in 1954 about 25 miles east-northeast of Houston, Texas, is a principal surface-water source for the city of Houston. The increase in water supply to meet future demands is expected to be accommodated by supplementing surface-water inflows to Lake Houston. The Trinity River is considered a potential source for interbasin transfer of water to Lake Houston. Before beginning to supplement inflows, the City needs to better understand the potential effects on Lake Houston water quality from streams that flow into or might contribute water to Lake Houston. During 1983–90, the USGS collected 3,727 water-quality samples from 27 sites in Lake Houston, 6 of the 7 main tributaries to the lake, and the Trinity River at Romayor.
\nLongitudinal profiles of water temperature, dissolved oxygen, specific conductance, pH, and nutrients from the dam to the East and West Forks of Lake Houston constructed for a winter day and a summer day indicate that in general the lake water is mixed in the winter and stratified in the summer.
\nThe results of Mann-Whitney rank-sum tests to determine whether there were significant differences between summer and non-summer field measurements, 5-day biological oxygen demand, bacteria, physical and aesthetic properties, nutrients, organic carbon, chlorophyll a, and trace elements in the lake nearest the dam, the East Fork of the lake, and the West Fork of the lake at the same relative depth showed significant differences between summer and non-summer samples for at least one of the three locations at the same relative depth for all 15 properties and constituents tested except specific conductance. The test results indicate that in general Lake Houston is well mixed in the non-summer period and stratified with respect to selected properties and constituents in the summer.
\nThe results of rank-sum tests to determine whether there were significant differences between field measurements, 5-day biological oxygen demand, physical and aesthetic properties, nutrients, organic carbon, and chlorophyll a in the lake nearest the dam, the East Fork of the lake, and the West Fork of the lake for samples collected during the same season at the same relative depth showed that significant differences were common; generally, the West Fork had the largest median concentrations among the three locations. The tests comparing trace element concentrations between the lake nearest the dam and the East Fork showed mixed results—large median dissolved manganese concentrations in lake bottom samples in the summer and in East Fork near-surface samples in the non-summer period.
\nThe results of rank-sum tests comparing selected properties, 5-day biological oxygen demand, bacteria, nutrients, and total organic carbon in the eastern tributaries with those in the western tributaries, in the eastern tributaries with those in the Trinity River, and in the western tributaries with those in the Trinity River during the same season (summer or non-summer) at the same relative streamflow (low-medium or high) showed that significant differences were more common than not. In the comparisons of the eastern tributaries with the western tributaries that resulted in significant differences, medians of the western tributaries were larger for all properties and constituents except total organic carbon; in the comparisons of the eastern tributaries with the Trinity River that resulted in significant differences, medians were larger for the Trinity River in about 60 percent of the tests; and in the comparisons of the western tributaries with the Trinity River that resulted in significant differences, medians were larger for the western tributaries in about 60 percent of the tests.
\nIn the tests comparing trace elements between the eastern and western tributaries during the same season at the same relative streamflow, five of the eight tests showed no significant differences; between the eastern tributaries and the Trinity River, all eight tests showed significant differences, with eastern tributary medians larger in all tests; and between the western tributaries and the Trinity River, seven of the eight tests showed significant differences, with western tributary medians larger in all seven tests.
\nThe tests comparing selected properties, 5-day biological oxygen demand, nutrients, and total organic carbon between the eastern tributaries and the East Fork of Lake Houston, between the western tributaries and the West Fork of Lake Houston, and between the Trinity River and the lake nearest the dam, the East Fork, and the West Fork during the same season (summer or nonsummer) yielded significant differences in about 60 percent of the tests. No discernible pattern emerged to associate significant differences with season.
\nIn the tests comparing trace elements between the tributaries and the respective forks of the lake to which the tributaries drain, iron concentrations were significantly different in three of the four tests, with median concentrations larger in the tributaries. All the tests comparing manganese between the Trinity River and the three locations in the lake yielded significant differences, with larger median concentrations in the lake.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Austin, TX","doi":"10.3133/wri994129","collaboration":"Prepared in cooperation with the City of Houston","usgsCitation":"Liscum, F., Goss, R., and Rast, W., 1999, Characteristics of water-quality data for Lake Houston, selected tributary inflows to Lake Houston, and the Trinity River near Lake Houston (a potential source of interbasin transfer), August 1983-September 1990: U.S. Geological Survey Water-Resources Investigations Report 99-4129, iv, 56 p., https://doi.org/10.3133/wri994129.","productDescription":"iv, 56 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":426340,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_22509.htm","linkFileType":{"id":5,"text":"html"}},{"id":2283,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri99-4129/","linkFileType":{"id":5,"text":"html"}},{"id":326611,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri994129.JPG"}],"country":"United States","state":"Texas","otherGeospatial":"Lake Houston, Trinity River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -95.5,\n 30.5\n ],\n [\n -95.5,\n 29.75\n ],\n [\n -94.75,\n 29.75\n ],\n [\n -94.75,\n 30.5\n ],\n [\n -95.5,\n 30.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e3727","contributors":{"authors":[{"text":"Liscum, Fred","contributorId":95463,"corporation":false,"usgs":true,"family":"Liscum","given":"Fred","email":"","affiliations":[],"preferred":false,"id":199733,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Goss, R.L.","contributorId":83143,"corporation":false,"usgs":true,"family":"Goss","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":199732,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rast, Walter","contributorId":79514,"corporation":false,"usgs":true,"family":"Rast","given":"Walter","affiliations":[],"preferred":false,"id":199731,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":25794,"text":"wri984113 - 1999 - Surface-water-quality assessment of the Yakima River basin, Washington: Overview of major findings, 1987-91","interactions":[],"lastModifiedDate":"2021-12-01T19:33:59.256418","indexId":"wri984113","displayToPublicDate":"2001-01-01T00:00:00","publicationYear":"1999","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":"98-4113","title":"Surface-water-quality assessment of the Yakima River basin, Washington: Overview of major findings, 1987-91","docAbstract":"Surface-water-quality conditions were assessed in the Yakima River Basin, which drains 6,155 square miles of mostly forested, range, and agricultural land in Washington. The Yakima River Basin is one of the most intensively farmed and irrigated areas in the United States, and is often referred to as the “Nation’s Fruitbowl.” Natural and anthropogenic sources of contaminants and flow regulation control water-quality conditions throughout the basin. This report summarizes the spatial and temporal distribution, sources, and implications of the dissolved oxygen, water temperature, pH, suspended sediment, nutrient, organic compound (pesticide), trace element, fecal indicator bacteria, radionuclide, and aquatic ecology data collected during the 1987–91 water years.
\nThe Yakima River descends from a water surface altitude of 2,449 feet at the foot of Keechelus Dam to 340 feet at its mouth downstream from Horn Rapids Dam near Richland. The basin can be divided into three distinct river reaches on the basis of its physical characteristics. The upper reach, which drains the Kittitas Valley, has a high gradient, with an average streambed slope of 14 feet per mile (ft/mi) over the 74 miles from the foot of Keechelus Dam (river mile [RM] 214.5) to just upstream from Umtanum. The middle reach, which drains the Mid Valley, extends a distance of 33 miles from Umtanum (RM 140.4) to just upstream from Union Gap and also has a high gradient, with an average streambed slope of 11 ft/mi. The lower reach of the Yakima River drains the Lower Valley and has an average streambed slope of 7 ft/mi over the 107 miles from Union Gap (RM 107.2) to the mouth of the Yakima River.
\nThese reaches exhibited differences in water-quality conditions related to the differences in geologic sources of contaminants and land use. Compared with the rest of the basin, the Kittitas Valley and headwaters of the Naches River Subbasin had relatively low concentrations and loads of suspended sediment, nutrients, organic compounds, and fecal indicator bacteria. There were very few failures to meet the Washington State dissolved oxygen standard or exceedances of the water temperature and pH standards in this reach. In general, these areas are considered to be areas of lessdegraded water quality in the basin. The preTertiary metamorphic and intrusive rocks of the Cle Elum and Teanaway River Subbasins, however, were found to be significant geologic sources of antimony, arsenic, chromium, copper, mercury, nickel, selenium, and zinc. As a result, the arsenic, chromium, and nickel concentrations measured in the streambed sediment of the Kittitas Valley were 13 to 74 times higher than those measured in the Lower Valley.
\nThe Mid and Lower Valleys had similar water-quality conditions, governed by the intensive agricultural and irrigation activities, highly erosive landscapes, and flow regulation. Most of the failures to meet the Washington State standards for dissolved oxygen and exceedances of the standards for water temperature and pH occurred in the Mid and Lower Valleys. Agricultural drains in the Mid and Lower Valleys were found to be significant sources of nutrients, suspended sediment, pesticides, and fecal indicator bacteria. Downstream from the irrigation diversions near Union Gap, summertime streamflow in the Yakima River was drastically reduced to only a few hundred cubic feet per second. In the lower Yakima River, agricultural return flow typically accounts for as much as 80 percent of the main stem summertime flow near the downstream terminus of the basin. Therefore, the water-quality characteristics of the lower Yakima River resemble those of the agricultural drains. The highest fecal bacteria concentrations (35,000 colonies of Escherichia coli per 100 milliliters of water) were measured in the Granger/Sunnyside area, the location of most of the livestock in the basin. The east side area of the Lower Valley (area east of the Yakima River) was the predominant source area for suspended sediment and pesticides in the basin. This area had the largest acreage of irrigated land and generally received the largest application of pesticides. Owing to the highly erosive soils of the area, the suspended sediment load from the east side in June 1989 (320 kilograms per day) was five or more times larger than from any other area, and the loads of several of the more hydrophobic organic compounds were four or more times larger.
\nAn ecological assessment of the Yakima River Basin ranked physical, chemical, and biological conditions at impaired (degraded) sites against reference sites in an effort to understand how land use changes physical and chemical site characteristics and how biota respond to these changes. For this assessment, the basin was divided into four natural ecological categories: (1) Cascades ecoregion, (2) Eastern Cascades Slopes and Foothills ecoregion, (3) Columbia Basin ecoregion, and (4) large rivers. Each of these categories has a unique combination of climate and landscape features that produces a distinctive terrestrial vegetation assemblage. In the combined Cascades and Eastern Cascades site group, which had the fewest impaired sites, the metals index was the only physical and chemical index that indicated any impairment. The moderate levels of impairment noted in the invertebrate and algal communities were not, however, associated with metals, and may have been related to the effects of logging, although the intensity of logging was not directly quantified in this study. Sites in the Columbia Basin site group were all moderately or severely impaired with the exception of the two reference sites (Umtanum Creek and Satus Creek below Dry Creek), which showed no physical, chemical, or biological impairment. Three sites were heavily affected by agriculture (Granger Drain, Moxee Drain, and Spring Creek) and were listed as severely impaired by most of the physical, chemical, and biological condition indices. Agriculture was the primary cause of the impairment of biological communities in this site group. The primary physical and chemical indicators of agricultural effects were nutrients, pesticides, dissolved solids, and substrate embeddedness, which all tended to increase with agricultural intensity. The biological effects of agriculture were manifested by a decrease in the abundance and number of native species of fish and invertebrates, a shift in algal communities to species indicative of eutrophic conditions, and higher abundances. There was also an increase in the abundance and number of nonnative fish species due to the prevalence of fish that are largely tolerant of nutrient-rich conditions. Main stem (large river) sites downstream from the city of Yakima exhibited severe impairment of fish communities associated with high levels of pesticides in fish tissues and the presence of external anomalies on fish.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Portland, OR","doi":"10.3133/wri984113","usgsCitation":"Morace, J.L., Fuhrer, G.J., Rinella, J.F., McKenzie, S.W., Gannett, M.W., Bramblett, K.L., Pogue, T.R., Skach, K.A., Embrey, S.S., Cuffney, T.F., Meador, M., Porter, S.D., and Gurtz, M.E., 1999, Surface-water-quality assessment of the Yakima River basin, Washington: Overview of major findings, 1987-91: U.S. Geological Survey Water-Resources Investigations Report 98-4113, xii, 119 p., https://doi.org/10.3133/wri984113.","productDescription":"xii, 119 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":158370,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri984113.PNG"},{"id":392338,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_19724.htm"},{"id":311182,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1998/4113/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Washington","otherGeospatial":"Yakima River Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.25885009765625,\n 46.057985244793024\n ],\n [\n -121.25885009765625,\n 46.90524554642923\n ],\n [\n -119.58892822265626,\n 46.90524554642923\n ],\n [\n -119.58892822265626,\n 46.057985244793024\n ],\n [\n -121.25885009765625,\n 46.057985244793024\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae5e4b07f02db68a896","contributors":{"authors":[{"text":"Morace, Jennifer L. 0000-0002-8132-4044 jlmorace@usgs.gov","orcid":"https://orcid.org/0000-0002-8132-4044","contributorId":945,"corporation":false,"usgs":true,"family":"Morace","given":"Jennifer","email":"jlmorace@usgs.gov","middleInitial":"L.","affiliations":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195099,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fuhrer, Gregory J. gjfuhrer@usgs.gov","contributorId":944,"corporation":false,"usgs":true,"family":"Fuhrer","given":"Gregory","email":"gjfuhrer@usgs.gov","middleInitial":"J.","affiliations":[],"preferred":true,"id":195098,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rinella, Joseph F. jrinella@usgs.gov","contributorId":1371,"corporation":false,"usgs":true,"family":"Rinella","given":"Joseph","email":"jrinella@usgs.gov","middleInitial":"F.","affiliations":[],"preferred":true,"id":195100,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"McKenzie, Stuart W.","contributorId":27841,"corporation":false,"usgs":true,"family":"McKenzie","given":"Stuart","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":195102,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Gannett, Marshall W. 0000-0003-2498-2427 mgannett@usgs.gov","orcid":"https://orcid.org/0000-0003-2498-2427","contributorId":2942,"corporation":false,"usgs":true,"family":"Gannett","given":"Marshall","email":"mgannett@usgs.gov","middleInitial":"W.","affiliations":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":true,"id":579616,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Bramblett, Karen L.","contributorId":149798,"corporation":false,"usgs":false,"family":"Bramblett","given":"Karen","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":579617,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Pogue, Ted R. 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