Twenty-one wells were drilled at Crossley Farms Superfund Site between December 15, 1987, and May 1, 1988, to define and monitor the horizontal and vertical distribution of ground-water contamination emanating from a suspected contaminant source area (Blackhead Hill). Eight well clusters were drilled on or near the Crossley Site and three well clusters were drilled at locations hydrologically down gradient from the site. Depths of wells range from 21 to 299 feet below land surface. These wells were installed in saprolite in shallow, intermediate, and deep water-producing zones of the fractured bedrock aquifer.
Borehole-geophysical and video logging were conducted between April 24, 1997, and May 8, 1997, to determine the water-producing zones, water-receiving zones, zones of vertical flow, borehole depth, and casing integrity in each well. This data and interpretation will be used to determine the location of the well intake for the existing open-hole wells, which will be retrofitted to isolate and monitor water-producing zones and prevent further cross-contamination within each open borehole, and identify wells that may need rehabilitation or replacement.
Caliper and video logs were used to locate fractures, inflections on fluid-temperature and fluid-resistivity logs indicated possible fluid-bearing fractures, and flowmeter measurements verified these locations. Single-point-resistance and natural-gamma logs provided information on stratigraphy. After interpretation of geophysical logs, video logs, and driller's notes, all wells will be constructed so that water-level fluctuations can be monitored and discrete water samples collected from shallow, intermediate, and deep water-bearing zones in each well.
Geophysical logs were run on seven bedrock and two deep bedrock wells. Gamma logs were run on 10 bedrock wells. Twenty-two wells were inspected visually with the borehole video camera for casing integrity.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr9862","issn":"0094-9140","collaboration":"Prepared in cooperation with the U.S. Environmental Protection Agency","usgsCitation":"Conger, R.W., 1998, Evaluation of geophysical logs, phase I, for Crossley Farms Superfund Site, Berks County, Pennsylvania: U.S. Geological Survey Open-File Report 98-62, v, 26 p. :ill., col. map ;28 cm., https://doi.org/10.3133/ofr9862.","productDescription":"v, 26 p. :ill., col. map ;28 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":350707,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1998/0062/ofr19980062.pdf","text":"Report","size":"646 KB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 1998-0062"},{"id":157050,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1998/0062/coverthb.jpg"}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
This Protocol is designed to evaluate the fate in ground water of chlorinated aliphatic hydrocarbons and/or fuel hydrocarbons. Documentation of natural attenuation requires detailed site characterization. The data collected under this protocol can be used to compare the relative effectiveness of other remedial options. and natural attenuation. This protocol should be used to evaluate whether monitored natural attenuation by itself or in conjunction with other remedial technologies is sufficient to achieve site-specific remedial objectives. Understanding the contaminant flow field in the subsurface is essential for a technically justified evaluation of a monitored natural attenuation remedial option; therefore, use of this protocol is not appropriate for evaluating monitored natural attenuation at sites where the contaminant flow field cannot be determined with an acceptable degree of certainty (e.g., complex fractured bedrock, karst, aquifers.)
Ground-water levels, predevelopment ground-water flow, and stream-aquifer relations in the vicinity of the U.S. Department of Energy Savannah River Site, Georgia and South Carolina, were evaluated as part of a cooperative study between the U.S. Geological Survey, U.S. Department of Energy, and Georgia Department of Natural Resources. As part of this evaluation: (1) ground-water-level fluctuations and trends in three aquifer systems in sediment of Cretaceous and Tertiary age were described and related to patterns of ground-water use and precipitations; (2) a conceptual model ofthe stream-aquifer flow system was developed; (3) the predevelopment ground-water flow system, configuration of potentiometric surfaces, trans-river flow, and recharge-discharge relations were described; and (4) stream-aquifer relations and the influence of river incision on ground-water flow and stream-aquifer relations were described. The 5,147-square mile study area is located in the northern part of the Coastal Plain physiographic province of Georgia and South Carolina. Coastal Plain sediments comprise three aquifer systems consisting of seven aquifers that are separated hydraulically by confining units. The aquifer systems are, in descending order: (1) the Floridan aquifer system?consisting of the Upper Three Runs and Gordon aquifers in sediments of Eocene age; (2) the Dublin aquifer system?consisting of the Millers Pond, upper Dublin, and lower Dublin aquifers in sediments of Paleocene-Late Cretaceous age; and (3) the Midville aquifer system?consisting of the upper Midville and lower Midville aquifers in sediments of Late Cretaceous age. The Upper Three Runs aquifer is the shallowest aquifer and is unconfined to semi-confined throughout most of the study area. Ground-water levels in the Upper Three Runs aquifer respond to a local flow system and are affected mostly by topography and climate. Ground-water flow in the deeper, Gordon aquifer and Dublin and Midville aquifer systems is characterized by local flow near outcrop areas to the north, changing to intermediate flow and then regional flow downdip (southeastward) as the aquifers become more deeply buried. Water levels in these deeper aquifers show a pronounced response to topography and climate in the vicinity of outcrops, and diminish southeastward where the aquifer is more deeply buried. Stream stage and pumpage affect ground-water levels in these deeper aquifers to varying degrees throughout the study area. The geologic characteristics of the Savannah River alluvial valley substantially control the configuration of potentiometric surfaces, ground-water-flow directions, and stream-aquifer relations. Data from 18 shallow borings indicate incision into each aquifer by the paleo Savannah River channel and subsequent infill of permeable alluvium, allowing for direct hydraulic connection between aquifers and the Savannah River along parts of its reach. This hydraulic connection may be the cause of large ground-water discharge to the river near Jackson, S.C., where the Gordon aquifer is in contact with Savannah River alluvium, and also the cause of lows or depressions formed in the potentiometric surfaces of confined aquifers that are in contact with the alluvium. Ground water in these aquifers flows toward the depressions. The influence of the river is diminished downstream where the aquifers are deeply buried, and upstream and downstream ground-water flow is possibly separated by a water divide or 'saddle'. Water-level data indicate that saddle features probably exist in the Gordon aquifer and Dublin aquifer system, and also might be present in the Midville aquifer system. Ground-water levels respond seasonally or in long term to changes in precipitation, evapotranspiration, pumpage, and river stage.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri974197","usgsCitation":"Clarke, J.S., and West, C.T., 1998, Ground-water levels, predevelopment ground-water flow, and stream-aquifer relations in the vicinity of the Savannah River Site, Georgia and South Carolina: U.S. Geological Survey Water-Resources Investigations Report 97-4197, ix, 118 p. , https://doi.org/10.3133/wri974197.","productDescription":"ix, 118 p. ","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":118784,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_97_4197.jpg"},{"id":1981,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri974197/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Georgia, South Carolina","otherGeospatial":"Savannah River Site","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -81.88385009765625,\n 33.091541548655236\n ],\n [\n -81.38946533203124,\n 33.091541548655236\n ],\n [\n -81.38946533203124,\n 33.332823028503576\n ],\n [\n -81.88385009765625,\n 33.332823028503576\n ],\n [\n -81.88385009765625,\n 33.091541548655236\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db69815d","contributors":{"authors":[{"text":"Clarke, John S. jsclarke@usgs.gov","contributorId":400,"corporation":false,"usgs":true,"family":"Clarke","given":"John","email":"jsclarke@usgs.gov","middleInitial":"S.","affiliations":[{"id":316,"text":"Georgia Water Science Center","active":true,"usgs":true}],"preferred":true,"id":196653,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"West, Christopher T.","contributorId":77547,"corporation":false,"usgs":true,"family":"West","given":"Christopher","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":196654,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28337,"text":"wri974211 - 1998 - Assessment of the hydraulic connection between ground water and the Peace River, west-central Florida","interactions":[],"lastModifiedDate":"2023-01-04T22:27:23.598961","indexId":"wri974211","displayToPublicDate":"1998-07-01T00:00:00","publicationYear":"1998","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":"97-4211","title":"Assessment of the hydraulic connection between ground water and the Peace River, west-central Florida","docAbstract":"The hydraulic connection between the Peace River and the underlying aquifers along the length of the Peace River from Bartow to Arcadia was assessed to evaluate flow exchanges between these hydrologic systems. Methods included an evaluation of hydrologic and geologic records and seismic-reflection profiles, seepage investigations, and thermal infrared imagery interpretation. Along the upper Peace River, a progressive long-term decline in streamflow has occurred since 1931 due to a lowering of the potentiometric surface of the Upper Floridan aquifer by as much as 60 feet because of intensive ground-water withdrawals for phosphate mining and agriculture. Another effect from lowering the potentiometric surface has been the cessation of flow at several springs located near and within the Peace River channel, including Kissengen Spring, that once averaged a flow of about 19 million gallons a day. The lowering of ground-water head resulted in flow reversals at locations where streamflow enters sinkholes along the streambed and floodplain.
Hydrogeologic conditions along the Peace River vary from Bartow to Arcadia. Three distinctive hydrogeologic areas along the Peace River were delineated: (1) the upper Peace River near Bartow, where ground-water recharge occurs; (2) the middle Peace River near Bowling Green, where reversals of hydraulic gradients occur; and (3) the lower Peace River near Arcadia, where ground-water discharge occurs.
Seismic-reflection data were used to identify geologic features that could serve as potential conduits for surface-water and ground-water exchange. Depending on the hydrologic regime, this exchange could be recharge of surface water into the aquifer system or discharge of ground water into the stream channel. Geologic features that would provide pathways for water movement were identified in the seismic record; they varied from buried irregular surfaces to large-scale subsidence flexures and vertical fractures or enlarged solution conduits. Generally, the upper Peace River is characterized by a shallow, buried irregular top of rock, numerous observed sinkholes, and subsidence depressions. The downward head gradient provides potential for the Peace River to lose water to the ground-water system. Along the middle Peace River area, head gradients alternate between downward and upward, creating both recharging and discharging ground-water conditions. Seismic records show that buried, laterally continuous reflectors in the lower Peace River pinch out in the middle Peace River streambed. Small springs have been observed along the streambed where these units pinch out. This area corresponds to the region where highest ground-water seepage volumes were measured during this study. Further south, along the lower Peace River, upward head gradients provide conditions for ground-water discharge into the Peace River. Generally, confinement between the surficial aquifer and the confined ground-water systems in this area is better than to the north. However, localized avenues for surface-water and ground-water interactions may exist along discontinuities observed in seismic reflectors associated with large-scale flexures or subsidence features.
Ground-water seepage gains or losses along the Peace River were quantified by making three seepage runs during periods of: (1) low base flow, (2) high base flow, and (3) high flow. Low and high base-flow seepage runs were performed along a 74-mile length of the Peace River, between Bartow and Nocatee. Maximum losses of 17.3 cubic feet per second (11.2 million gallons per day) were measured along a 3.2-mile reach of the upper Peace River. The high-flow seepage run was conducted to quantify losses in the Peace River channel and floodplain between Bartow and Fort Meade. Seepage losses calculated during high-flow along a 7.2-mile reach of the Peace River, from the Clear Springs Mine bridge to the Mobil Mine bridge, were approximately 10 percent of the river flow, or 118 cubic feet per second. Calculated seepages along the Peace River in Hardee and De Soto Counties were inconclusive, because most seepages were within the range of discharge measurement error.
Two continuous aerial thermal infrared imagery surveys were conducted to locate sites of ground-water discharge along the Peace River. Although temperature and hydrologic conditions were ideal to observe spring flow using thermal infrared imaging techniques, no sources of ground-water discharge were identified using this method. Diffuse ground-water seepage may, however, provide significant ground-water discharge.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri974211","usgsCitation":"Lewelling, B., Tihansky, A., and Kindinger, J., 1998, Assessment of the hydraulic connection between ground water and the Peace River, west-central Florida: U.S. Geological Survey Water-Resources Investigations Report 97-4211, vi, 96 p., https://doi.org/10.3133/wri974211.","productDescription":"vi, 96 p.","costCenters":[],"links":[{"id":2249,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri974211/","linkFileType":{"id":5,"text":"html"}},{"id":120163,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_97_4211.jpg"},{"id":411395,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48820.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","otherGeospatial":"Peace River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -81.9375,\n 27.9214\n ],\n [\n -81.9375,\n 27.1428\n ],\n [\n -81.75,\n 27.1428\n ],\n [\n -81.75,\n 27.9214\n ],\n [\n -81.9375,\n 27.9214\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671d24","contributors":{"authors":[{"text":"Lewelling, B. R.","contributorId":17969,"corporation":false,"usgs":true,"family":"Lewelling","given":"B. R.","affiliations":[],"preferred":false,"id":199616,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tihansky, A. B. 0000-0003-1681-1601","orcid":"https://orcid.org/0000-0003-1681-1601","contributorId":77956,"corporation":false,"usgs":true,"family":"Tihansky","given":"A. B.","affiliations":[],"preferred":false,"id":199618,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kindinger, J. L.","contributorId":38983,"corporation":false,"usgs":true,"family":"Kindinger","given":"J. L.","affiliations":[],"preferred":false,"id":199617,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":23555,"text":"ofr96209 - 1998 - Simulation of ground-water flow in the Albuquerque Basin, central New Mexico, 1901-95, with projections to 2020","interactions":[],"lastModifiedDate":"2012-02-02T00:08:09","indexId":"ofr96209","displayToPublicDate":"1998-07-01T00:00:00","publicationYear":"1998","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":"96-209","title":"Simulation of ground-water flow in the Albuquerque Basin, central New Mexico, 1901-95, with projections to 2020","docAbstract":"The ground-water-flow model of the Albuquerque Basin (Kernodle, \r\nJ.M., McAda, D.P., and Thorn, C.R., 1995, Simulation of ground-water flow \r\nin the Albuquerque Basin, central New Mexico, with projections to \r\n2020: U.S. Geological Survey Water-Resources Investigations Report \r\n94-4251, 114 p.) was updated to include new information on the \r\nhydrogeologic framework (Hawley, J.W., Haase, C.S., and Lozinsky, \r\nR.P., 1995, An underground view of the Albuquerque Basin: Proceedings \r\nof the 39th Annual New Mexico Water Conference, November 3-4, 1994,\r\np. 37-55). An additional year of ground-water-withdrawal data was \r\nappended to the simulation of the historical period and incorporated \r\ninto the base for future projections to the year 2020. The revised \r\nmodel projects the simulated ground-water levels associated with an \r\naerally enlarged occurrence of the relatively high hydraulic conductivity \r\nin the upper part of the Santa Fe Group east and west of the Rio Grande \r\nin the Albuquerque area and north to Bernalillo. Although the differences \r\nbetween the two model versions are substantial, the revised model does not \r\ncontradict any previous conclusions about the effect of City of Albuquerque \r\nground-water withdrawals on flow in the Rio Grande or the net benefits \r\nof an effort to conserve ground water. Recent revisions to the hydrogeologic \r\nmodel (Hawley, J.W., Haneberg, W.C., and Whitworth, P.M., in press, \r\nHydrogeologic investigations in the Albuquerque Basin, central New Mexico, \r\n1992-1995: Socorro, New Mexico Bureau of Mines and Mineral Resources Open- \r\nFile Report 402) of the Albuquerque Basin eventually will require that this \r\nmodel version also be revised and updated.","language":"ENGLISH","publisher":"U.S. Geological Survey, [Water Resources Division, New Mexico District],","doi":"10.3133/ofr96209","issn":"0094-9140","usgsCitation":"Kernodle, J.M., 1998, Simulation of ground-water flow in the Albuquerque Basin, central New Mexico, 1901-95, with projections to 2020: U.S. Geological Survey Open-File Report 96-209, v, 54 p. :ill., maps ;28 cm., https://doi.org/10.3133/ofr96209.","productDescription":"v, 54 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":156533,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0209/report-thumb.jpg"},{"id":52847,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0209/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f8e4b07f02db5f2aa5","contributors":{"authors":[{"text":"Kernodle, J. M.","contributorId":81139,"corporation":false,"usgs":true,"family":"Kernodle","given":"J.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":190309,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":21754,"text":"ofr98127 - 1998 - Drainage from adits and tailings piles in the Coeur d'Alene mining district, Idaho; sampling, analytical methods and results","interactions":[],"lastModifiedDate":"2019-05-10T08:52:17","indexId":"ofr98127","displayToPublicDate":"1998-07-01T00:00:00","publicationYear":"1998","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":"98-127","title":"Drainage from adits and tailings piles in the Coeur d'Alene mining district, Idaho; sampling, analytical methods and results","docAbstract":"This report contains information about collecting, handling, and analyzing waters draining from adits and seeping from beneath tailings piles in the Coeur d'Alene mining district during August 1996, November 1996, and June 1997. Data include temperature, pH, conductivity, dissolved oxygen, alkalinity, flow, and total acid soluble and dissolved (<0.45 \\im) major and trace ion concentrations for 11 adits and 5 tailings deposits. Interpretations of these data will be discussed in other publications.
","language":"English","publisher":"U.S. Geological Survey,","publisherLocation":"Reston, VA","doi":"10.3133/ofr98127","issn":"0566-8174","usgsCitation":"Balistrieri, L.S., Bookstrom, A., Box, S.E., and Ikramuddin, M., 1998, Drainage from adits and tailings piles in the Coeur d'Alene mining district, Idaho; sampling, analytical methods and results: U.S. Geological Survey Open-File Report 98-127, 19 p., https://doi.org/10.3133/ofr98127.","productDescription":"19 p.","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":51255,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1998/0127/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":152991,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1998/0127/report-thumb.jpg"}],"country":"United States","state":"Idaho","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a61e4b07f02db635f5a","contributors":{"authors":[{"text":"Balistrieri, Laurie S. 0000-0002-6359-3849 balistri@usgs.gov","orcid":"https://orcid.org/0000-0002-6359-3849","contributorId":1406,"corporation":false,"usgs":true,"family":"Balistrieri","given":"Laurie","email":"balistri@usgs.gov","middleInitial":"S.","affiliations":[{"id":200,"text":"Coop Res Unit Seattle","active":true,"usgs":true},{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true},{"id":662,"text":"Western Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"preferred":true,"id":762437,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bookstrom, A. A.","contributorId":94681,"corporation":false,"usgs":true,"family":"Bookstrom","given":"A. A.","affiliations":[],"preferred":false,"id":185547,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Box, S. E.","contributorId":38567,"corporation":false,"usgs":true,"family":"Box","given":"S.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":185544,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ikramuddin, Mohammed","contributorId":46115,"corporation":false,"usgs":true,"family":"Ikramuddin","given":"Mohammed","email":"","affiliations":[],"preferred":false,"id":185545,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":6644,"text":"fs00398 - 1998 - Changes in sediment and nutrient storage in three reservoirs in the lower Susquehanna River Basin and implications for the Chesapeake Bay","interactions":[],"lastModifiedDate":"2018-02-20T14:26:05","indexId":"fs00398","displayToPublicDate":"1998-04-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":313,"text":"Fact Sheet","code":"FS","onlineIssn":"2327-6932","printIssn":"2327-6916","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"003-98","title":"Changes in sediment and nutrient storage in three reservoirs in the lower Susquehanna River Basin and implications for the Chesapeake Bay","docAbstract":"The Susquehanna River contributes nearly 50 percent of the freshwater discharge to the Chesapeake Bay in a year of normal or average streamflow. The river also transports the greatest amount of nutrients (estimates of nearly 66 percent of the nitrogen and 40 percent of the phosphorus load) from all nontidal areas in the Chesapeake Bay Basin. Excessive nutrients in the Bay result in algal blooms that decrease the amount of light reaching submerged aquatic vegetation, and upon decomposition, deplete the oxygen in the water. In a normal-flow year, the Susquehanna River also contributes about 25 percent of the sediment load from non-tidal areas to the Bay. Suspended sediments also reduce light needed by submerged aquatic vegetation and can smother living-resource habitat and obstruct fish gills.
A reservoir system consisting of Lake Clarke, Lake Aldred, and Conowingo Reservoir is formed by three consecutive hydroelectric dams on the Lower Susquehanna River. Safe Harbor Dam, which forms Lake Clarke, was built in 1931. Holtwood Dam, the smallest of the three, was built in 1910 to form Lake Aldred. The largest and most downstream dam, Conowingo Dam, was built in 1928 and forms Conowingo Reservoir. Since construction, the reservoirs have been filling with sediment and sediment-associated nutrients. The upper two reservoirs have reached their capacity to store sediments and generally no longer trap nutrients and sediments. Conowingo Reservoir has not reached storage capacity, however, and is currently trapping about 70 percent of the suspended-sediment load, 2 percent of the total-nitrogen load, and 40 percent of the total-phosphorus load that would otherwise be discharged to the Chesapeake Bay (Ott and others, 1991).
In 1990, 1993, and 1996, the U.S. Geological Survey collected information on the depth to sediment in the reservoirs to determine the remaining sediment-storage capacity in the reservoir system and to estimate when the reservoirs will reach sediment-storage capacity. In addition, sediment cores were collected and analyzed in 1993 and 1996 to determine the nutrient mass remaining in the Conowingo Reservoir. The 1996 data collection followed a major flood in the Susquehanna River Basin.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/fs00398","usgsCitation":"Langland, M.J., 1998, Changes in sediment and nutrient storage in three reservoirs in the lower Susquehanna River Basin and implications for the Chesapeake Bay: U.S. Geological Survey Fact Sheet 003-98, 4 p., https://doi.org/10.3133/fs00398.","productDescription":"4 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":121629,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/fs/1998/0003/coverthb2.jpg"},{"id":34070,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/fs/1998/0003/fs19980003.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}}],"contact":"Director, Pennsylvania Water Science Center
U.S. Geological Survey
215 Limekiln Road
New Cumberland, PA 17070
Approximately 170 Mgal/d (million gallons per day) of ground- and surface-water was withdrawn from the Barataria-Terrebonne Basins in 1995. Of this amount, surface water accounted for 64 percent ( 110 MgaVd) of the total withdrawal rates in the basins. The largest surface-water withdrawal rates were from Bayou Lafourche ( 40 Mgal/d), Bayou Boeuf ( 14 MgaVd), and the Gulf Intracoastal Waterway (4.2 Mgal/d). The largest ground-water withdrawal rates were from the Mississippi River alluvial aquifer (29 Mgal/d), the Gonzales-New Orleans aquifer (9.5 Mgal/d), and the Norco aquifer (3.6 MgaVd).
\n\nThe amounts of water withdrawn in the basins in 1995 differed by category of use. Public water suppliers within the basins withdrew 41 Mgal/d of water. The five largest public water suppliers in the basins withdrew 30 Mgal/d of surface water: Terrebonne Waterworks District 1 withdrew the largest amount, almost 15 MgaVd. Industrial facilities withdrew 88 Mgal/d, fossil-fuel plants withdrew 4.7 MgaVd, and commercial facilities withdrew 0.67 MgaVd. Aggregate water-withdrawal rates, compiled by parish for aquaculture (37 Mgal/d), livestock (0.56 Mgal/d), rural domestic (0.44 MgaVd), and irrigation uses (0.54 MgaVd), totaled about 38 MgaVd in the basins. Ninety-five percent of aquaculture withdrawal rates, primarily for crawfish and alligator farming, were from surface-water sources.
\n\n>br>\n\nTotal water-withdrawal rates increased 221 percent from 1960–95. Surface-water withdrawal rates have increased by 310 percent, and ground-water withdrawal rates have increased by 133 percent. The projection for the total water-withdrawal rates in 2020 is 220 MgaVd, an increase of 30 percent from 1995. Surface-water withdrawal rates would account for 59 percent of the total, or 130 Mgal/d. Surface-water withdrawal rates are projected to increase by 20 percent from 1995 to 2020.
\n\nAnalysis of water-quality data from the Mississippi River indicates that the main threats to surface water resources are from the herbicide atrazine and excessive nutrients. Atrazine concentrations in the Mississippi River at Baton Rouge briefly exceed the U.S. Environmental Protection Agency maximum contaminant level of 3.0 micrograms per liter during periods in the late spring and early summer. Trace metals in bottom material collected from Bayou Lafourche indicate that the reach of Bayou Lafourche from Donaldsonville to Golden Meadow is adversely affected by low-level contamination. Dissolved nitrate had a mean concentration of 1.4 milligrams per liter in the Mississippi River near Bayou Lafourche and can contribute to excessive plant growth.
\n\nLong-term salinity records near Bayou Lafourche indicate no pronounced trends, with the exception of the Gulf Intracoastal Waterway at Houma. At this site, salinities remained low until 1961, when the Gulf Intracoastal Waterway was connected to the Gulf of Mexico by the Houma Navigation Canal. The sources of saltwater are variable. Some saltwater has entered Bayou Lafourche south of the Gulf Intracoastal Waterway; at other times saltwater has moved up the Houma Navigation Canal and has flowed east in the Gulf Intracoastal Waterway, north into Company Canal, and southeast in Bayou Lafourche towards Larose, Louisiana.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr98632","issn":"0094-9140","collaboration":"Prepared in cooperation with the Barataria-Terrebonne National Estuary Program","usgsCitation":"Johnson-Thibaut, P.M., Demcheck, D.K., Swarzenski, C.M., and Ensminger, P.A., 1998, Water use and quality of fresh surface-water resources in the Barataria-Terrebonne Basins, Louisiana: U.S. Geological Survey Open-File Report 98-632, Report: iv, 47 p.; 1 Map: 24.00 x 18.00 inches, https://doi.org/10.3133/ofr98632.","productDescription":"Report: iv, 47 p.; 1 Map: 24.00 x 18.00 inches","numberOfPages":"52","onlineOnly":"Y","costCenters":[{"id":369,"text":"Louisiana Water Science Center","active":true,"usgs":true}],"links":[{"id":430164,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_16372.htm","linkFileType":{"id":5,"text":"html"}},{"id":283814,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1998/ofr98-632/pdf/of1998-632_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":283812,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1998/ofr98-632/","linkFileType":{"id":1,"text":"pdf"}},{"id":283813,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1998/ofr98-632/pdf/of1998-632.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":283816,"rank":4,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Louisiana","otherGeospatial":"Barataria-Terrebonne Basins","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -91.81954122716522,\n 30.762616503019416\n ],\n [\n -91.81954122716522,\n 29.036394388511\n ],\n [\n -89.743022989434,\n 29.036394388511\n ],\n [\n -89.743022989434,\n 30.762616503019416\n ],\n [\n -91.81954122716522,\n 30.762616503019416\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f004f","contributors":{"authors":[{"text":"Johnson-Thibaut, Penny M.","contributorId":10830,"corporation":false,"usgs":true,"family":"Johnson-Thibaut","given":"Penny","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":187941,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Demcheck, Dennis K. 0000-0003-2981-078X ddemchec@usgs.gov","orcid":"https://orcid.org/0000-0003-2981-078X","contributorId":3273,"corporation":false,"usgs":true,"family":"Demcheck","given":"Dennis","email":"ddemchec@usgs.gov","middleInitial":"K.","affiliations":[],"preferred":true,"id":187939,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Swarzenski, Christopher M. 0000-0001-9843-1471 cswarzen@usgs.gov","orcid":"https://orcid.org/0000-0001-9843-1471","contributorId":656,"corporation":false,"usgs":true,"family":"Swarzenski","given":"Christopher","email":"cswarzen@usgs.gov","middleInitial":"M.","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":17705,"text":"Wetland and Aquatic Research Center","active":true,"usgs":true}],"preferred":true,"id":187938,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ensminger, Paul A. 0000-0002-0536-0369 paensmin@usgs.gov","orcid":"https://orcid.org/0000-0002-0536-0369","contributorId":4754,"corporation":false,"usgs":true,"family":"Ensminger","given":"Paul","email":"paensmin@usgs.gov","middleInitial":"A.","affiliations":[{"id":24708,"text":"Lower Mississippi-Gulf Water Science Center","active":true,"usgs":true}],"preferred":true,"id":187940,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70181805,"text":"70181805 - 1998 - Intercomparison of principal hydrometric instruments; Third phase, Evaluation of ultrasonic velocity meters for flow measurement in streams, canals, and estuaries","interactions":[],"lastModifiedDate":"2017-02-14T13:27:48","indexId":"70181805","displayToPublicDate":"1998-03-10T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"title":"Intercomparison of principal hydrometric instruments; Third phase, Evaluation of ultrasonic velocity meters for flow measurement in streams, canals, and estuaries","docAbstract":"As part of the World Meteorological Organization (WMO) project Intercomparison of Principal Hydrometric Instruments, Third Phase, a questionnaire was prepared by the U.S. Geological Survey (USGS) on the application of Ultrasonic Velocity Meters (UVM's) for flowmeasurement in streams, canals, and estuaries. In 1996, this questionnaire was distributed internationally by the WMO and USGS, and distributed within the United States by the USGS. Completed questionnaires were returned by 26 agencies in 7 countries (Canada, France, Germany, The Netherlands, Switzerland, the United Kingdom, and the United States). The completed questionnaires described geometric and streamflow conditions, system configurations, and reasons for applying UVM systems for 260 sites, thus providing information on the applicability of UVM systems throughout the world. The completed questionnaires also provided information on operational issues such as (1) methods used to determine and verify UVM ratings, (2) methods used to determine the mean flow velocity for UVM systems, (3) operational reliability of UVM systems, (4) methods to estimate missing data, (5) common problems with UVM systems and guidelines to mitigate these problems, and (6) personnel training issues. The completed questionnaires also described a few unique or novel applications of UVM systems. In addition to summarizing the completed questionnaires, this report includes a brief overview of UVM application and operation, and a short summary of current (1998) information from UVM system manufacturers regarding system cost and capabilities. On the basis of the information from the completed questionnaires and provided by the manufacturers, the general applicability of UVM systems is discussed. In the finalisation of this report the financial support provided by the US National Committee for Scientific Hydrology is gratefully acknowledged.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"WMO/TD","largerWorkSubtype":{"id":4,"text":"Other Government Series"},"language":"English","publisher":"World Meteorological Organization","publisherLocation":"Geneva, Switzerland","usgsCitation":"Melching, C.S., and Meno, M.W., 1998, Intercomparison of principal hydrometric instruments; Third phase, Evaluation of ultrasonic velocity meters for flow measurement in streams, canals, and estuaries.","costCenters":[],"links":[{"id":335363,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58a4253be4b0c825128ad481","contributors":{"authors":[{"text":"Melching, Charles S.","contributorId":8135,"corporation":false,"usgs":true,"family":"Melching","given":"Charles","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":668648,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Meno, Michael W.","contributorId":181570,"corporation":false,"usgs":false,"family":"Meno","given":"Michael","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":668649,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5871,"text":"pp1573 - 1998 - Sediment transport at gaging stations near Mount St. Helens, Washington, 1980-90. Data collection and analysis","interactions":[],"lastModifiedDate":"2021-12-21T21:01:30.440904","indexId":"pp1573","displayToPublicDate":"1998-03-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1573","title":"Sediment transport at gaging stations near Mount St. Helens, Washington, 1980-90. Data collection and analysis","docAbstract":"River sedimentation caused by the May 18, 1980, eruption of Mount St. Helens, Washington, has been monitored in a continuing program by the U.S. Geological Survey. In this report, sediment discharge and changes in sediment transport are summarized from data collected at stream-gaging stations near Mount St. Helens during the years 1980 through 1990. The objectives of the monitoring program included collection of data for calculation of total sediment discharge, computation of daily suspended-sediment discharge, and detailed observations of unique sediment-laden flows. Over the 11-year period, most sediment data were collected at gaging stations on seven eruption affected streams: the Green River, the North and South Fork Toutle Rivers, the Toutle River, the Cowlitz River, Clearwater Creek, and the Muddy River.
\nAbout 170 million tons of sediment (excluding volcanic debris flows) were transported in suspension from the Toutle River basin during water years 1980–90. Another 13 million tons were transported past the gaging stations on Muddy River in the upper Lewis River basin during water years 1982–90. Long-term reductions in sediment concentration occurred within most ranges of stream discharge at streams dominated by transport from the debris-avalanche deposit and at streams in drainage basins with extensive airfall deposits. Reductions in sediment concentration were less apparent at upper ranges of discharge in two streams dominated by lahar deposits, the South Fork Toutle River and the Muddy River.
\nBed material, suspended sediment, and bedload were sampled periodically and analyzed for size distributions. Bed material and bedload coarsened with time at some stations. Median particle sizes of suspended sediment did not show a simple relation with time. During water years 1980–84, bed material in the lower Toutle River was medium to coarse sand. During the same period, bed material in the North Fork Toutle River was coarse sand and fine gravel. By 1990, bedload samples collected in the North Fork Toutle River (downstream from the sediment-retention structure) were typically coarse gravel.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1573","usgsCitation":"Dinehart, R.L., 1998, Sediment transport at gaging stations near Mount St. Helens, Washington, 1980-90. Data collection and analysis (Revised June 5, 2008): U.S. Geological Survey Professional Paper 1573, Report: x, 105 p.; Readme, https://doi.org/10.3133/pp1573.","productDescription":"Report: x, 105 p.; Readme","numberOfPages":"118","additionalOnlineFiles":"Y","costCenters":[{"id":157,"text":"Cascades Volcano Observatory","active":false,"usgs":true},{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":279267,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":393255,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13148.htm"},{"id":279266,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/pp/1573/readme.htm"},{"id":32685,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1573/pdf/PP1573.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":713,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1573/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Washington","otherGeospatial":"Clearwater Creek, Cowlitz River, Green River, Mount St. Helens, Muddy River, North Fork Toutle River, South Fork Toutle River, Toutle River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.95,\n 46.05\n ],\n [\n -121.95,\n 46.05\n ],\n [\n -121.95,\n 46.583\n ],\n [\n -122.95,\n 46.583\n ],\n [\n -122.95,\n 46.05\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Revised June 5, 2008","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbf3d","contributors":{"authors":[{"text":"Dinehart, Randal L.","contributorId":21151,"corporation":false,"usgs":true,"family":"Dinehart","given":"Randal","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":151713,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":6447,"text":"pp1424D - 1998 - Hydrogeologic framework of the Puget Sound aquifer system, Washington and British Columbia","interactions":[{"subject":{"id":22198,"text":"ofr96353 - 1997 - Summary of the Puget-Willamette Lowland regional aquifer-system analysis, Washington, Oregon, and British Columbia","indexId":"ofr96353","publicationYear":"1997","noYear":false,"title":"Summary of the Puget-Willamette Lowland regional aquifer-system analysis, Washington, Oregon, and British Columbia"},"predicate":"SUPERSEDED_BY","object":{"id":6447,"text":"pp1424D - 1998 - Hydrogeologic framework of the Puget Sound aquifer system, Washington and British Columbia","indexId":"pp1424D","publicationYear":"1998","noYear":false,"chapter":"D","title":"Hydrogeologic framework of the Puget Sound aquifer system, Washington and British Columbia"},"id":1}],"lastModifiedDate":"2023-01-06T19:24:24.551204","indexId":"pp1424D","displayToPublicDate":"1998-03-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1424","chapter":"D","title":"Hydrogeologic framework of the Puget Sound aquifer system, Washington and British Columbia","docAbstract":"This report presents the generalized hydrogeologic framework of the Puget Sound aquifer system in Washington and British Columbia. The framework includes a conceptual model of the division of the aquifer system into regional hydrogeologic units for describing on a regional basis the ground-water flow in the system. The conceptual model is based on an analysis of historical data and on results of cross-sectional numerical models of ground-water flow.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1424D","usgsCitation":"Vaccaro, J.J., Hansen, A.J., and Jones, M., 1998, Hydrogeologic framework of the Puget Sound aquifer system, Washington and British Columbia: U.S. Geological Survey Professional Paper 1424, Report: vii, 77 p.; 1 Plate: 40.00 x 32.00 inches, https://doi.org/10.3133/pp1424D.","productDescription":"Report: vii, 77 p.; 1 Plate: 40.00 x 32.00 inches","costCenters":[],"links":[{"id":411508,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13145.htm","linkFileType":{"id":5,"text":"html"}},{"id":33866,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1424d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33865,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1424d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":118182,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1424d/report-thumb.jpg"}],"country":"Canada, United States","state":"British Columbia, Washington","otherGeospatial":"Puget Sound aquifer system","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -124.06132108981615,\n 49.254548392531206\n ],\n [\n -124.06132108981615,\n 46.980785167463864\n ],\n [\n -121.87752582623631,\n 46.980785167463864\n ],\n [\n -121.87752582623631,\n 49.254548392531206\n ],\n [\n -124.06132108981615,\n 49.254548392531206\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ee4b07f02db627a14","contributors":{"authors":[{"text":"Vaccaro, J. J.","contributorId":48173,"corporation":false,"usgs":true,"family":"Vaccaro","given":"J.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":152737,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hansen, Arnold J. Jr.","contributorId":84336,"corporation":false,"usgs":true,"family":"Hansen","given":"Arnold","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":152738,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jones, M. A.","contributorId":37736,"corporation":false,"usgs":true,"family":"Jones","given":"M. A.","affiliations":[],"preferred":false,"id":152736,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70047752,"text":"70047752 - 1998 - Hydrology and snowmelt simulation of Snyderville Basin, Park City, and adjacent areas, Summit County, Utah","interactions":[],"lastModifiedDate":"2017-01-05T17:07:47","indexId":"70047752","displayToPublicDate":"1998-01-01T15:32:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":294,"text":"Technical Publication","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"115","title":"Hydrology and snowmelt simulation of Snyderville Basin, Park City, and adjacent areas, Summit County, Utah","docAbstract":"Increasing residential and commercial development is placing increased demands on the ground- and surface-water resources of Snyderville Basin, Park City, and adjacent areas in the southwestern corner of Summit County, Utah. Data collected during 1993-95 were used to assess the quantity and quality of the water resources in the study area.
Ground water within the study area is present in consolidated rocks and unconsolidated valley fill. The complex geology makes it difficult to determine the degree of hydraulic connection between different blocks of consolidated rocks. Increased ground-water withdrawal during 1983- 95 generally has not affected ground-water levels. Ground-water withdrawal in some areas, however, caused seasonal fluctuations and a decline in ground-water levels from 1994 to 1995, despite greater-than-normal recharge in the spring of 1995.
Ground water generally has a dissolved-solids concentration that ranges from 200 to 600 mg/L. Higher sulfate concentrations in water from wells and springs near Park City and in McLeod Creek and East Canyon Creek than in other parts of the study area are the result of mixing with water that discharges from the Spiro Tunnel. The presence of chloride in water from wells and springs near Park City and in streams and wells near Interstate Highway 80 is probably caused by the dissolution of applied road salt. Chlorofluorocarbon analyses indicate that even though water levels rise within a few weeks of snowmelt, the water took 15 to 40 years to move from areas of recharge to areas of discharge.
Water budgets for the entire study area and for six subbasins were developed to better understand the hydrologic system. Ground-water recharge from precipitation made up about 80 percent of the ground-water recharge in the study area. Ground-water discharge to streams made up about 40 percent of the surface water in the study area and ground-water discharge to springs and mine tunnels made up about 25 percent. Increasing use of ground water has the potential to decrease discharge to streams and affect both the amount and quality of surface water in the study area. A comparison of the 1995 to 1994 water budgets emphasizes that the hydrologic system in the study area is very dependent upon the amount of annual precipitation. Although precipitation on the study area was much greater in 1995 than in 1994, most of the additional water resulted in additional streamflow and spring discharge that flows out of the study area. Ground-water levels and groundwater discharge are dependent upon annual precipitation and can vary substantially from year to year.
Snowmelt runoff was simulated to assist in estimating ground-water recharge to consolidated rock and unconsolidated valley fill. A topographically distributed snowmelt model controlled by independent inputs of net radiation, meteorological parameters, and snowcover properties was used to calculate the energy and mass balance of the snowcover.
","language":"English","publisher":"Utah Department of Natural Resources, Division of Water Rights","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared by the United States Geological Survey in cooperation with the Utah Department of Natural Resources, Division of Water Rights; Park City; Summit County; and the Weber Basin Water Conservancy District","usgsCitation":"Brooks, L.E., Mason, J.L., and Susong, D.D., 1998, Hydrology and snowmelt simulation of Snyderville Basin, Park City, and adjacent areas, Summit County, Utah: Technical Publication 115, vi, 84 p.","productDescription":"vi, 84 p.","numberOfPages":"93","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":279943,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70047752/report.pdf"},{"id":279942,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70047752/report-thumb.jpg"},{"id":332236,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://www.waterrights.utah.gov/cgi-bin/libview.exe?Modinfo=Viewpub&LIBNUM=50-1-165"}],"scale":"100000","projection":"Universal Transverse Mercator projection","country":"United States","state":"Utah","county":"Summit County","city":"Park City","otherGeospatial":"East Canyon Creek;Mcleod Creek;Snyderville Basin;Spiro Tunnel","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -111.646973,40.599669 ], [ -111.646973,40.819739 ], [ -111.432945,40.819739 ], [ -111.432945,40.599669 ], [ -111.646973,40.599669 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"529dba1ce4b0516126f68cf3","contributors":{"authors":[{"text":"Brooks, Lynette E. 0000-0002-9074-0939 lebrooks@usgs.gov","orcid":"https://orcid.org/0000-0002-9074-0939","contributorId":2718,"corporation":false,"usgs":true,"family":"Brooks","given":"Lynette","email":"lebrooks@usgs.gov","middleInitial":"E.","affiliations":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"preferred":true,"id":482893,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mason, James L.","contributorId":14397,"corporation":false,"usgs":true,"family":"Mason","given":"James","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":482894,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Susong, David D. ddsusong@usgs.gov","contributorId":1040,"corporation":false,"usgs":true,"family":"Susong","given":"David","email":"ddsusong@usgs.gov","middleInitial":"D.","affiliations":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"preferred":true,"id":482892,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70093983,"text":"70093983 - 1998 - Hydrogeology and groundwater quality of the glaciated valleys of Bradford, Tioga, and Potter Counties, Pennsylvania","interactions":[],"lastModifiedDate":"2014-02-14T15:39:23","indexId":"70093983","displayToPublicDate":"1998-01-01T15:09:00","publicationYear":"1998","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":143,"text":"Water Resource Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"68","title":"Hydrogeology and groundwater quality of the glaciated valleys of Bradford, Tioga, and Potter Counties, Pennsylvania","docAbstract":"The most important sources of groundwater in Bradford, Tioga, and Potter Counties are the stratified-drift aquifers. Saturated sand and gravel primarily of outwash origin forms extensive unconfined aquifers in the valleys. Outwash is underlain in most major valleys by silt, clay, and very fine sand of lacustrine origin that comprise extensive confining units. The lacustrine confining units locally exceed 100 feet in thickness. Confined aquifers of ice-contact sand and gravel are buried locally beneath the lacustrine deposits. Bedrock and till are the basal confining units of the stratifies-drift aquifer systems. Recharge to the stratified-drift aquifers if by direct infiltration of precipitation, tributary-stream infiltration, infiltration of unchanneled runoff at the valley walls, and groundwater inflow from the bedrock and till uplands. Valley areas underlain by superficial sand and gravel contribute about 1 million gallons per day per square mile of water from precipitation to the aquifers. Tributary streams provide recharge of nearly 590 gallons per day per foot of stream reach. Water is added at the rate of 1 million gallons per day per square mile of bordering uplands not drained by tributary streams to the stratified-drift aquifers from unchanneled runoff and groundwater inflow. Induced infiltration can be a major source of recharge to well fields completed in unconfined stratified-drift aquifers that are in good hydraulic connection with surface water. The well fields of an industrial site in North Towanda, a public-water supplier at Tioga Point, and the U.S. Fish and Wildlife Service at Asaph accounted for 75 percent of the 10.8 million gallons per day pf groundwater withdrawn by public suppliers and other selected users in 1985. The well fields tap stratified-drift aquifers that are substantially recharged by induced infiltration or tributary-stream infiltration. Specific-capacity data from 95 wells indicate that most wells completed in stratified-drift aquifers have specific capacities an order of magnitude greater than those completed in till and bedrock, Wells completed in unconfined stratified-drift aquifers and in bedrock aquifers have the highest and lowest median specific capacities -- 24 and 0.80 gallons per minute per foot of drawdown, respectively. Wells completed in confined stratified-drift aquifers and in till have median specific capacties of 11 and 0.87 gallons per minute per foot of drawdown, respectively. The results of 223 groundwater-quality analyses indicate two major hydrogeochemical zones: (1) a zone of unrestricted groundwater flow that contains water of the calcium bicarbonate type (this zone is found in almost all of the stratified-drift aquifers, till, and shallow bedrock systems); and (2) a zone of restricted groundwater slow that contains water of the sodium chloride type (this zone is found in the bedrock, and, in some areas, in till and confined stratified-drift aquifers). Samples pumped from wells that penetrate restricted-flow zones have median concentrations of total dissolved solids, dissolved chloride, and dissolved barium of 840 and 350 milligrams per liter, and 2,100 micrograms per liter, respectively. Excessive concentrations of iron and manganese are common in the groundwater of the study area; about 50 percent of the wells sampled contain water that has iron and manganese concentrations that exceed the U.S. Environmental Protection Agency secondary maximum contaminant levels of 300 and 50 micrograms per liter, respectively. Only water in the unconfined stratified-drift aquifers and the Catskill Formation has median concentrations lower than these limits.","language":"English","publisher":"Pennsylvania Geological Survey","publisherLocation":"Harrisburg, PA","isbn":"081820169X","collaboration":"Prepared by the United States Geological Survey, Water Resources Division, in cooperation with the Pennsylvania Geological Survey","usgsCitation":"Williams, J., Taylor, L.E., and Low, D.J., 1998, Hydrogeology and groundwater quality of the glaciated valleys of Bradford, Tioga, and Potter Counties, Pennsylvania: Water Resource Report 68, v, 89 p.","productDescription":"v, 89 p.","numberOfPages":"98","costCenters":[],"links":[{"id":282437,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Pennsylvania","county":"Bradford County;Potter County;Tioga County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -78.367676,41.542419 ], [ -78.367676,42.002415 ], [ -76.101494,42.002415 ], [ -76.101494,41.542419 ], [ -78.367676,41.542419 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd6125e4b0b290850fd5c2","contributors":{"authors":[{"text":"Williams, John 0000-0002-6054-6908 jhwillia@usgs.gov","orcid":"https://orcid.org/0000-0002-6054-6908","contributorId":1553,"corporation":false,"usgs":true,"family":"Williams","given":"John","email":"jhwillia@usgs.gov","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":true,"id":490413,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Taylor, Larry E.","contributorId":73920,"corporation":false,"usgs":true,"family":"Taylor","given":"Larry","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":490415,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Low, Dennis J. djlow@usgs.gov","contributorId":3450,"corporation":false,"usgs":true,"family":"Low","given":"Dennis","email":"djlow@usgs.gov","middleInitial":"J.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":490414,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70021102,"text":"70021102 - 1998 - Salinity trends in surface waters of the Upper Colorado River Basin, Colorado","interactions":[],"lastModifiedDate":"2024-03-29T11:20:35.700744","indexId":"70021102","displayToPublicDate":"1998-01-01T00:00:00","publicationYear":"1998","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2262,"text":"Journal of Environmental Quality","active":true,"publicationSubtype":{"id":10}},"title":"Salinity trends in surface waters of the Upper Colorado River Basin, Colorado","docAbstract":"Dissolved-solids data collected in the Upper Colorado River Basin upstream from Cameo, Colorado, and in the Gunnison River Basin were analyzed for trends in flow-adjusted dissolved-solids concentrations and loads for water years 1970 to 1993, 1980 to 1993, and 1986 to 1993. Trend results for flow-adjusted periodic dissolved-solids concentrations for the Colorado River Basin upstream from Cameo, CO, generally were downward or no trend was indicated. Trends in flow-adjusted monthly and annual dissolved-solids loads primarily were downward or absent. These trend results partly agree with the downward trends reported by a previous investigation for the Colorado River near Cameo site. In the Gunnison River Basin, trends in flow-adjusted dissolved-solids concentrations and loads were not detected for more than one-half of the site/analysis-period combinations. Of the trends that were present, most indicated decreases in concentrations and loads rather than increases. In both the Colorado River Basin upstream from Cameo, CO, and the Gunnison River Basin, trends in flow-adjusted dissolved-solids concentrations and flow-adjusted monthly and annual dissolved-solids loads may be affected by a variety of factors. These include channel evolution and hydrologic variation, water quality and flow rate of groundwater discharges and springs, sample size and period of record of dissolved-solids data, and changes in land use in the basin.
In this, the second of two papers concerned with the use of numerical simulation to examine flow and transport parameters in heterogeneous porous media via Monte Carlo methods, results from the transport aspect of these simulations are reported on. Transport simulations contained herein assume a finite pulse input of conservative tracer, and the numerical technique endeavors to realistically simulate tracer spreading as the cloud moves through a heterogeneous medium. Medium heterogeneity is limited to the hydraulic conductivity field, and generation of this field assumes that the hydraulic-conductivity process is second-order stationary. Methods of estimating cloud moments, and the interpretation of these moments, are discussed. Techniques for estimation of large-time macrodispersivities from cloud second-moment data, and for the approximation of the standard errors associated with these macrodispersivities, are also presented. These moment and macrodispersivity estimation techniques were applied to tracer clouds resulting from transport scenarios generated by specific Monte Carlo simulations. Where feasible, moments and macrodispersivities resulting from the Monte Carlo simulations are compared with first- and second-order perturbation analyses. Some limited results concerning the possible ergodic nature of these simulations, and the presence of non-Gaussian behavior of the mean cloud, are reported on as well.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/97WR02711","usgsCitation":"Naff, R., Haley, D., and Sudicky, E., 1998, High-resolution Monte Carlo simulation of flow and conservative transport in heterogeneous porous media: 2. Transport results: Water Resources Research, v. 34, no. 4, p. 679-697, https://doi.org/10.1029/97WR02711.","productDescription":"19 p.","startPage":"679","endPage":"697","costCenters":[],"links":[{"id":229695,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"34","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a30fae4b0c8380cd5db16","contributors":{"authors":[{"text":"Naff, R.L.","contributorId":86349,"corporation":false,"usgs":true,"family":"Naff","given":"R.L.","affiliations":[],"preferred":false,"id":388586,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Haley, D.F.","contributorId":68480,"corporation":false,"usgs":true,"family":"Haley","given":"D.F.","email":"","affiliations":[],"preferred":false,"id":388585,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sudicky, E.A.","contributorId":67237,"corporation":false,"usgs":true,"family":"Sudicky","given":"E.A.","email":"","affiliations":[],"preferred":false,"id":388584,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}