{"pageNumber":"290","pageRowStart":"7225","pageSize":"25","recordCount":11003,"records":[{"id":31700,"text":"ofr96632 - 1996 - Physical characteristics of stream subbasins in the Hawk Creek-Yellow Medicine River basin, southwestern Minnesota and eastern South Dakota","interactions":[],"lastModifiedDate":"2018-04-02T10:11:15","indexId":"ofr96632","displayToPublicDate":"1997-09-01T00:00:00","publicationYear":"1996","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":"96-632","title":"Physical characteristics of stream subbasins in the Hawk Creek-Yellow Medicine River basin, southwestern Minnesota and eastern South Dakota","docAbstract":"<p>Data that describe the physical characteristics of stream subbasins upstream from selected sites on streams in the Hawk Creek-Yellow Medicine River Basin, located in southwestern Minnesota and eastern South Dakota are presented in this report. The physical characteristics are the drainage area of the subbasin, the percentage area of the subbasin covered only by lakes, the percentage area of the subbasin covered by both lakes and wetlands, the main-channel length, and the main-channel slope. Stream sites include outlets of subbasins of at least 5 square miles, outlets of sewage treatment plants, and locations of U.S. Geological Survey low-flow, high-flow, and continuous-record gaging stations.</p>","language":"English","publisher":"United States","publisherLocation":"Denver, CO","doi":"10.3133/ofr96632","collaboration":"Prepared in cooperation with Minnesota Department of Transportation","usgsCitation":"Sanocki, C.A., 1996, Physical characteristics of stream subbasins in the Hawk Creek-Yellow Medicine River basin, southwestern Minnesota and eastern South Dakota: U.S. Geological Survey Open-File Report 96-632, Document: 21 p.; Plate: 44 x 36 inches, https://doi.org/10.3133/ofr96632.","productDescription":"Document: 21 p.; Plate: 44 x 36 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":19525,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1996/0632/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":160868,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0632/report-thumb.jpg"},{"id":19526,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0632/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota, South Dakota","otherGeospatial":"Hawk Creek-Yellow Medicine River basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -95.87699890136719, 45.02355322956419 ], [ -95.86463928222656, 45.02840634444917 ], [ -95.86395263671875, 45.034229539203075 ], [ -95.85708618164062, 45.045389006413735 ], [ -95.83717346191406, 45.03956694724904 ], [ -95.83580017089842, 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,{"id":5163,"text":"fs21596 - 1996 - Salinity in the Colorado River in the Grand Valley, western Colorado, 1994-95","interactions":[],"lastModifiedDate":"2017-06-30T10:43:19","indexId":"fs21596","displayToPublicDate":"1997-09-01T00:00:00","publicationYear":"1996","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":"215-96","title":"Salinity in the Colorado River in the Grand Valley, western Colorado, 1994-95","docAbstract":"Salinity, or the dissolved-solids concentration, is the measure of salts such as sodium chloride, calcium bicarbonate, and calcium sulfate that are dissolved in water. About one-half of the salinity in the Colorado River Basin is from natural sources (U.S. Department of the Interior, 1995), such as thermal springs in the Glenwood-Dotsero area, located about 90 miles upstream from Grand Junction (fig. 1). Effects of human activities, such as irrigation, reservoir evaporation, and transbasin diversions, have increased the levels of salinity in the Colorado River. High salinity can affect industrial and municipal water users by causing increased water-treatment costs, increased deterioration of plumbing and appliances, increased soap needs, and undesirable taste of drinking water. High salinity also can cause lower crop yields by reducing water and nutrient uptake by plants and can increase agricultural production costs because of higher leaching and drainage requirements. Agricultural losses might occur when salinity reaches about 700?850 milligrams per liter (U.S Department of the Interior, 1994).  Figure 1. Irrigated area in the Grand Valley and locations of sampling sites for the 1994?95 salinity study of the Colorado River. The Colorado River is the major source of irrigation water to the Grand Valley (fig. 1) and also is one source of water for the Clifton Water District, which supplies domestic water to part of the eastern Grand Valley. During spring and early summer in 1994, the Colorado River in the Grand Valley had lower than average streamflow. There was concern by water users about the effect of this low streamflow on salinity in the river. In 1994, the U.S. Geological Survey (USGS), in cooperation with the Colorado River Water Conservation District, began a study to evaluate salinity in the Colorado River. This fact sheet describes results of that study. The specific objectives of the fact sheet are to (1) compare salinity in the Colorado River among different locations from Cameo to the Colorado-Utah State line, (2) assess variations in salinity for different times of the year, and (3) describe the relation between streamflow and salinity in the river.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/fs21596","usgsCitation":"Butler, D.L., and von Guerard, P.B., 1996, Salinity in the Colorado River in the Grand Valley, western Colorado, 1994-95: U.S. Geological Survey Fact Sheet 215-96, 1 sheet (4 p.) : col. ill., col. map ; 28 cm. col. ill., col. map ;, https://doi.org/10.3133/fs21596.","productDescription":"1 sheet (4 p.) : col. ill., col. map ; 28 cm. col. ill., col. map ;","costCenters":[],"links":[{"id":124927,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/fs_215_96.bmp"},{"id":582,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/fs-215-96/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Colorado","otherGeospatial":"Grand Valley","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -108.42269897460938,\n              39.15349256868936\n            ],\n            [\n              -107.72781372070312,\n              39.15349256868936\n            ],\n            [\n              -107.72781372070312,\n              39.606746222241476\n            ],\n            [\n              -108.42269897460938,\n              39.606746222241476\n            ],\n            [\n              -108.42269897460938,\n              39.15349256868936\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4880e4b07f02db515edc","contributors":{"authors":[{"text":"Butler, David L.","contributorId":12843,"corporation":false,"usgs":true,"family":"Butler","given":"David","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":150527,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"von Guerard, Paul B.","contributorId":15601,"corporation":false,"usgs":true,"family":"von Guerard","given":"Paul","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":150528,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":22054,"text":"ofr96732 - 1996 - Preliminary report on the distribution of modern fauna and flora at selected sites in north-central and north-eastern Florida Bay","interactions":[],"lastModifiedDate":"2020-03-27T06:58:12","indexId":"ofr96732","displayToPublicDate":"1997-08-01T00:00:00","publicationYear":"1996","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":"96-732","title":"Preliminary report on the distribution of modern fauna and flora at selected sites in north-central and north-eastern Florida Bay","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96732","issn":"0094-9140","usgsCitation":"Brewster-Wingard, G., Ishman, S., Edwards, L.E., and Willard, D., 1996, Preliminary report on the distribution of modern fauna and flora at selected sites in north-central and north-eastern Florida Bay: U.S. Geological Survey Open-File Report 96-732, 34 p. , https://doi.org/10.3133/ofr96732.","productDescription":"34 p. ","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":153089,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":1223,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pdf/of/ofr96732.html","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              -87.5390625,\n              30.939924331023445\n            ],\n            [\n              -87.51708984375,\n              30.334953881988564\n            ],\n            [\n              -85.8251953125,\n              29.99300228455108\n            ],\n            [\n              -84.17724609375,\n              29.075375179558346\n            ],\n            [\n              -83.1884765625,\n              28.34306490482549\n            ],\n            [\n              -82.4853515625,\n              26.05678288577881\n            ],\n            [\n              -80.57373046875,\n              24.627044746156027\n            ],\n            [\n              -79.7607421875,\n              26.41155054662258\n            ],\n            [\n              -80.04638671875,\n              27.89734922968426\n            ],\n            [\n              -80.9912109375,\n              30.031055426540206\n            ],\n            [\n              -81.40869140625,\n              30.713503990354965\n            ],\n            [\n              -81.82617187499999,\n              30.80791068136646\n            ],\n            [\n              -84.814453125,\n              30.789036751261136\n            ],\n            [\n              -84.990234375,\n              31.109388560814963\n            ],\n            [\n              -87.5390625,\n              30.939924331023445\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66c98d","contributors":{"authors":[{"text":"Brewster-Wingard, G. L.","contributorId":102508,"corporation":false,"usgs":true,"family":"Brewster-Wingard","given":"G. L.","affiliations":[],"preferred":false,"id":186879,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ishman, S. E.","contributorId":20346,"corporation":false,"usgs":true,"family":"Ishman","given":"S. E.","affiliations":[],"preferred":false,"id":186877,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Edwards, Lucy E. 0000-0003-4075-3317 leedward@usgs.gov","orcid":"https://orcid.org/0000-0003-4075-3317","contributorId":2647,"corporation":false,"usgs":true,"family":"Edwards","given":"Lucy","email":"leedward@usgs.gov","middleInitial":"E.","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":186876,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Willard, Debra  A. 0000-0003-4878-0942","orcid":"https://orcid.org/0000-0003-4878-0942","contributorId":85982,"corporation":false,"usgs":true,"family":"Willard","given":"Debra  A.","affiliations":[],"preferred":false,"id":186878,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":32945,"text":"pp1410E - 1996 - Hydrology of the southeastern Coastal Plain aquifer system in South Carolina and parts of Georgia and North Carolina","interactions":[],"lastModifiedDate":"2017-01-11T10:27:03","indexId":"pp1410E","displayToPublicDate":"1997-08-01T00:00:00","publicationYear":"1996","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":"1410","chapter":"E","title":"Hydrology of the southeastern Coastal Plain aquifer system in South Carolina and parts of Georgia and North Carolina","docAbstract":"<p>The wedge of sediments present beneath the Coastal Plain of South Carolina and adjacent parts of Georgia and North Carolina consists of sand, silt, clay, and limestone. These strata have been subdivided into six regional aquifers: the surficial aquifer, the Floridan aquifer system, the Tertiary sand aquifer, the Black Creek aquifer, the Middendorf aquifer, and the Cape Fear aquifer. Intervening confining units separate the aquifers, except for the Floridan aquifer system and the Tertiary sand aquifer, which together function as a single hydrologic unit.</p>\n<p>The quality of ground water from the Coastal Plain aquifers of South Carolina generally is acceptable for most uses in most areas. The water in most aquifers under most of the Coastal Plain contains low concentrations of dissolved solids (less than 500 milligrams per liter) and no dominant constituents in the recharge areas. Downgradient, the water is a calcium bicarbonate or sodium bicarbonate type throughout most of the Coastal Plain. Sodium-chloride-type water is present still farther downgradient, near the coast.</p>\n<p>A quasi-three-dimensional, finite-difference digital ground-water flow model was constructed to simulate flow in the Coastal Plain aquifers prior to development. The model also was used to evaluate the hydraulic responses to pumping that have occurred up to November 1982. The model consisted of five layers and a 48 by 63 node grid with a uniform square grid cell of 4 miles on a side.</p>\n<p>The Coastal Plain aquifers are recharged primarily by precipitation in their outcrop areas. Discharge is primarily as base flow to upper Coastal Plain rivers, to overlying aquifers by leakage through confining units, and to wells.</p>\n<p>Total simulated flow in the deep ground-water system was 967 cubic feet per second at the end of the transient simulation (1982). Recharge to the deep flow system simulated by the model was 793 cubic feet per second in the study area in 1982. Simulated aquifer discharge to large rivers was 660 cubic feet per second. Discharge to smaller rivers was not simulated because of the scale of the model.</p>\n<p>Changes resulting from ground-water pumping were significant as of 1982. The simulated water budget indicates that in 1982, 249 cubic feet per second were discharged from the aquifer system by wells. This pumping was balanced by the following changes from predevelopment conditions: 110 cubic feet per second derived from storage, 67 cubic feet per second decrease in aquifer-to-river discharge, 44 cubic feet per second increase in net inflow from source-sinks, and a net increase in inflow of 28 cubic feet per second across boundaries. Head declines in the Black Creek and Middendorf aquifers have occurred throughout much of the eastern part of the Coastal Plain of South Carolina as a result of pumping in the Myrtle Beach and Florence areas. Simulation indicates that the dominant sources of water for upper Coastal Plain pumping centers such as the city of Florence are decrease in flow to rivers in the upper Coastal Plain and water derived from storage. The dominant sources of water for pumping centers in the Myrtle Beach area are water derived from storage, leakage from overlying aquifers, and net increases in inflow across boundaries.</p>\n<p>Transmissivity values used in the flow simulation range from less than 1,000 feet squared per day near the updip limit of most aquifers to about 30,000 feet squared per day in the Middendorf aquifer in the Savannah River Plant area. Vertical hydraulic conductivity values used in simulation of confining units range from about 6x10<sup>-7</sup> feet per day for the confining unit between the Middendorf and Black Creek aquifers in coastal areas to 3x10<sup>-2</sup> feet per day for most of the confining units near their updip limits. Storage coefficients used in transient simulations were 0.15 where unconfined conditions exist and 0.0005 where confined conditions exist.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/pp1410E","usgsCitation":"Aucott, W.R., 1996, Hydrology of the southeastern Coastal Plain aquifer system in South Carolina and parts of Georgia and North Carolina: U.S. Geological Survey Professional Paper 1410, vii, 83 p., https://doi.org/10.3133/pp1410E.","productDescription":"vii, 83 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":60848,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1410e/report.pdf","text":"Report","size":"22.81 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":121869,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1410e/report-thumb.jpg"}],"country":"United States","state":"Georgia, North Carolina, South Carolina","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -79.87060546875,\n              34.94899072578227\n            ],\n            [\n              -80.8154296875,\n              34.34343606848294\n            ],\n            [\n              -81.353759765625,\n              33.706062655101206\n            ],\n            [\n              -82.265625,\n              33.293803558346596\n            ],\n            [\n              -81.134033203125,\n              31.194007509998823\n            ],\n            [\n              -79.47509765625,\n              32.26855544621479\n            ],\n            [\n              -78.167724609375,\n              33.348884792201694\n            ],\n            [\n              -77.838134765625,\n              33.8339199536547\n            ],\n            [\n              -78.49731445312499,\n              34.97600151317591\n            ],\n            [\n              -79.12353515625,\n              35.60371874069731\n            ],\n            [\n              -79.87060546875,\n              34.94899072578227\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc79f","contributors":{"authors":[{"text":"Aucott, Walter R.","contributorId":90275,"corporation":false,"usgs":true,"family":"Aucott","given":"Walter","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":209493,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":23778,"text":"ofr96735 - 1996 - Coalbed methane potential in the Appalachian states of Pennsylvania, West Virginia, Maryland, Ohio, Virginia, Kentucky, and Tennessee; an overview","interactions":[],"lastModifiedDate":"2012-02-02T00:08:18","indexId":"ofr96735","displayToPublicDate":"1997-08-01T00:00:00","publicationYear":"1996","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":"96-735","title":"Coalbed methane potential in the Appalachian states of Pennsylvania, West Virginia, Maryland, Ohio, Virginia, Kentucky, and Tennessee; an overview","docAbstract":"This report focuses on the coalbed methane (CBM) potential of the central Appalachian basin (Virginia, eastern Kentucky, southern West Virginia, and Tennessee) and the northern Appalachian basin (Pennsylvania, northern West Virginia, Maryland, and Ohio). As of April 1996, there were about 800 wells producing CBM in the central and northern Appalachian basin. For the Appalchian basin as a whole (including the Cahaba coal field, Alabama, and excluding the Black Warrior Basin, Alabama), the total CBM production for 1992, 1993, 1994, and 1995, is here estimated at 7.77, 21.51, 29.99, and 32 billion cubic feet (Bcf), respectively. These production data compare with 91.38, 104.70, 110.70, and 112.11 Bcf, respectively, for the same years for the Black Warrior Basin, which is the second largest CBM producing basin in the United States. For 1992-1995, 92-95% of central and northern Appalachian CBM production came from southwestern Virginia, which has by far the largest CBM production the Appalachian states, exclusive of Alabama. For 1994, the average daily production of CBM wells in Virginia was 119.6 Mcf/day, which is about two to four times the average daily production rates for many of the CBM wells in the northern Appalachian basin.\r\n\r\nFor 1992-1995, there is a clear increase in the percentage of CBM being produced in the central and northern Appalachian basin as compared with the Black Warrior Basin. In 1992, this percentage was 8% of the combined central and northern Appalachian and Black Warrior Basin CBM production as compared with 22% in 1995. These trends imply that the Appalachian states, except for Alabama and Virginia, are in their infancy with respect to CBM production.\r\n\r\nTotal in place CBM resources in the central and northern Appalachian basin have been variously estimated at 66-76 trillion cubic feet (Tcf), of which an estimated 14.55 Tcf (3.07 Tcf for central Appalachian basin and 11.48 Tcf for northern Appalachian basin) is technically recoverable according to Ricei s (1995) report. This compares with 20 Tcf in place and 2.30 Tcf as technically recoverable CBM for the Black Warrior Basin. These estimates should be considered preliminary because of unknown CBM potential in Ohio, Maryland, Tennessee, and eastern Kentucky. The largest potential for CBM development in the central Appalachian basin is in the Pocahontas coal beds, which have total gas values as much as 700 cf/ton, and in the New River coal beds. In the northern Appalachian basin, the greatest CBM potential is in the Middle Pennsylvanian Allegheny coal beds, which have total gas values as much as 252 cf/ton. Rice (1995) estimated a mean estimated ultimate recovery per well of 521 MMcfg for the central Appalachian basin and means of 121 and 216 MMcfg for the anticlinal and synclinal areas, respectively, of the northern Applachian basin.\r\n\r\nThere is potential for CBM development in the Valley coal fields and Richmond basin of Virginia, the bituminous region of southeastern Kentucky, eastern Ohio, northern Tennessee, and the Georges Creek coal field of western Maryland and adjacent parts of Pennsylvania. Moreover, the Anthracite region of eastern Pennsylvania, which has the second highest known total gas content for a single coal bed (687 cf/ton) in the central and northern Appalachian basin, should be considered to have a fair to good potential for CBM development where structure, bed continuity, and permeability are favorable.\r\n\r\nCBM is mainly an undeveloped unconventional fossil-fuel resource in the central and northern Appalachian basin states, except in Virginia, and will probably contribute an increasing part of total Appalachian gas production into the next century as development in Pennsylvania, West Virginia, Ohio, and other Appalachian states continue. The central and northern Appalachian basins are frontier or emerging regions for CBM exploration and development, which will probably extend well into the next century. On the basis of CBM production ","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr96735","issn":"0094-9140","usgsCitation":"Lyons, P., 1996, Coalbed methane potential in the Appalachian states of Pennsylvania, West Virginia, Maryland, Ohio, Virginia, Kentucky, and Tennessee; an overview: U.S. Geological Survey Open-File Report 96-735, 66 p. :ill.; 28 cm., https://doi.org/10.3133/ofr96735.","productDescription":"66 p. :ill.; 28 cm.","costCenters":[],"links":[{"id":157392,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0735/report-thumb.jpg"},{"id":9124,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1996/of96-735/","linkFileType":{"id":5,"text":"html"}},{"id":53008,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0735/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6aec1b","contributors":{"authors":[{"text":"Lyons, Paul C.","contributorId":79894,"corporation":false,"usgs":true,"family":"Lyons","given":"Paul C.","affiliations":[],"preferred":false,"id":190709,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":25434,"text":"wri964138 - 1996 - Detailed study of selenium and other constituents in water, bottom sediment, soil, alfalfa, and biota associated with irrigation drainage in the Uncompahgre Project area and in the Grand Valley, west-central Colorado, 1991-93","interactions":[],"lastModifiedDate":"2025-01-08T14:26:25.607745","indexId":"wri964138","displayToPublicDate":"1997-07-01T00:00:00","publicationYear":"1996","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":"96-4138","title":"Detailed study of selenium and other constituents in water, bottom sediment, soil, alfalfa, and biota associated with irrigation drainage in the Uncompahgre Project area and in the Grand Valley, west-central Colorado, 1991-93","docAbstract":"<p>In 1985, the U.S. Department of the Interior began a program to study the effects of irrigation drainage in the Western United States. These studies were done to determine whether irrigation drainage was causing problems related to human health, water quality, and fish and wildlife resources. Results of a study in 1991-93 of irrigation drainage associated with the Uncompahgre Project area, located in the lower Gunnison River Basin, and of the Grand Valley, located along the Colorado River, are described in this report. The focus of the report is on the sources, distribution, movement, and fate of selenium in the hydrologic and biological systems and the effects on biota. Generally, other trace- constituent concentrations in water and biota were not elevated or were not at levels of concern. </p><p>Soils in the Uncompahgre Project area that primarily were derived from Mancos Shale contained the highest concentrations of total and watrer-extractable selenium. Only 5 of 128 alfalfa samples had selenium concentrations that exceeded a recommended dietary limit for livestock. Selenium data for soil and alfalfa indicate that irrigation might be mobilizing and redistributing selenium in the Uncompahgre Project area. </p><p>Distribution of dissolved selenium in ground water is affected by the aqueous geochemical environment of the shallow ground- water system. Selenium concentrations were as high as 1,300 micrograms per liter in water from shallow wells. The highest concentrations of dissolved selenium were in water from wells completed in alluvium overlying the Mancos Shale of Cretaceous age; selenium concentrations were lower in water from wells completed in Mancos Shale residuum. Selenium in the study area could be mobilized by oxidation of reduced selenium, desorption from aquifer sediments, ion exchange, and dissolution. Infiltration of irrigation water and, perhaps nitrate, provide oxidizing conditions for mobilization of selenium from alluvium and shale residuum and for transport to streams and irrigation drains that are tributary to the Gunnison, Uncompahgre, and Colorado Rivers. </p><p>Selenium concentrations in about 64 percent of water samples collected from the lower Gunnison River and about 50 percent of samples from the Colorado River near the Colorado-Utah State line exceeded the U.S. Environmental Protection Agency criterion of 5 micrograms per liter for protection of aquatic life. Almost all selenium concentrations in samples collected during the nonirrigation season from Mancos Shale areas exceeded the aquatic-life criterion. The maximum selenium concentrations in surface-water samples were 600 micrograms per liter in the Uncompahgre Project area and 380 micrograms per liter in the Grand Valley. </p><p>Irrigation drainage from the Uncompahgre Project and the Grand Valley might account for as much as 75 percent of the selenium load in the Colorado River near the Colorado-Utah State line. The primary source areas of selenium were the eastern side of the Uncompahgre Project and the western one-half of the Grand Valley, where there is extensive irrigation on soils derived from Mancos Shale. The largest mean selenium loads from tributary drainages were 14.0 pounds per day from Loutsenhizer Arroyo in the Uncompahgre Project and 12.8 pounds per day from Reed Wash in the Grand Valley. Positive correlations between selenium loads and dissolved-solids loads could indicate that salinity-control projects designed to decrease dissolved-solids loads also could decrease selenium loads from the irrigated areas. Selenium concentrations in irrigation drainage in the Grand Valley were much higher than concentrations predicted by simple evaporative concentration of irrigation source water. Selenium probably is removed from pond water by chemical and biological processes and incorporated into bottom sediment. The maximum selenium concentration in bottom sediment was 47 micrograms per gram from a pond on the eastern side of the Uncompahgre Project.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964138","usgsCitation":"Butler, D.L., Wright, W.G., Stewart, K.C., Osmundson, B.C., Krueger, R.P., and Crabtree, D., 1996, Detailed study of selenium and other constituents in water, bottom sediment, soil, alfalfa, and biota associated with irrigation drainage in the Uncompahgre Project area and in the Grand Valley, west-central Colorado, 1991-93: U.S. Geological Survey Water-Resources Investigations Report 96-4138, ix, 136 p., https://doi.org/10.3133/wri964138.","productDescription":"ix, 136 p.","costCenters":[],"links":[{"id":123072,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4138/report-thumb.jpg"},{"id":54166,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4138/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":465849,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48486.htm","text":"Grand Valley area","linkFileType":{"id":5,"text":"html"}},{"id":465850,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48487.htm","text":"Uncompahgre area","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b1e4b07f02db530813","contributors":{"authors":[{"text":"Butler, D. L.","contributorId":36967,"corporation":false,"usgs":true,"family":"Butler","given":"D.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":193676,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wright, W. G.","contributorId":19582,"corporation":false,"usgs":true,"family":"Wright","given":"W.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":193675,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stewart, K. C.","contributorId":46519,"corporation":false,"usgs":true,"family":"Stewart","given":"K.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":193677,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Osmundson, B. C.","contributorId":15655,"corporation":false,"usgs":true,"family":"Osmundson","given":"B.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":193674,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Krueger, R. P.","contributorId":8890,"corporation":false,"usgs":true,"family":"Krueger","given":"R.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":193672,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Crabtree, D.W.","contributorId":10070,"corporation":false,"usgs":true,"family":"Crabtree","given":"D.W.","email":"","affiliations":[],"preferred":false,"id":193673,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":29337,"text":"wri964038C - 1996 - Benthic invertebrates of benchmark streams in agricultural areas of eastern Wisconsin — Western Lake Michigan drainages","interactions":[],"lastModifiedDate":"2022-01-21T21:01:57.760672","indexId":"wri964038C","displayToPublicDate":"1997-07-01T00:00:00","publicationYear":"1996","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":"96-4038","chapter":"C","title":"Benthic invertebrates of benchmark streams in agricultural areas of eastern Wisconsin — Western Lake Michigan drainages","docAbstract":"<p>This study describes the benthic invertebrate communities of 20 benchmark streams in agricultural areas of eastern Wisconsin. Streams with minimal adverse effects from human activity were selected from four agricultural areas with differing surficial deposits and bedrock types (relatively homogeneous units, or RHU's). Most aquatic invertebrate orders were well represented in the 20 benchmark stream samples; 217 species and 151 genera within 56 families were identified. Diptera was the best represented order (96 species), followed by Trichoptera (42 species) and Ephemeroptera (26 species). Diptera were the most abundant organisms in terms of numbers of individuals in the sample (28 percent of the total) followed by Trichoptera (25 percent) and Ephemeroptera (13 percent). Nine species of freshwater mussels were found, but only in 5 of the 20 benchmark streams.</p>\n<p>Community measures were calculated for the following: total number of individuals; number of species; number of families; Margalef's diversity index; percent dominant family; percent Ephemeroptera-Plecoptera-Trichoptera (EPT); ratio of EPT to Chironomidae; percent shredders; ratio of scrapers to collectors-gatherers-filterers; Hilsenhoff's Biotic Index; Hilsenhoff's family level biotic index; and mean tolerance value. The S AS statistical software package was used for calculations of variance and correlations, normality checks, and principal components analysis of these measures and to find relations between benthic-invertebrate data and environmental-setting, habitat, and water-quality data.</p>\n<p>Coefficients of variation within the RHU's were as great or greater than those for all 20 streams for most measures and RHU's. The specific taxa assemblages present at the sites did not show distinct differences between RHU's or similarities within the RHU's. The covariance and the Kruskal-Wallis tests showed that the benthic invertebrate measures were not related to RHU. These results all indicate that the combined effect of the RHU variables (bedrock geology, texture of surficial deposits, and land use/land cover) were not elemental in describing invertebrate communities in the study-area streams.</p>\n<p>A principal components analysis (PCA) was done on the 20 benchmark streams which used the invertebrate population measures as variables. A three-dimensional ordination plot of these components revealed that 18 of the 20 streams could be divided into three groups relative to stream size, available habitat, and water quality. The three classifications of streams include large, warmer streams with slight pollution; deep, mixed-water streams with minimal pollution; and small, cold, pristine headwater streams. The two streams not defined by the three PCA groupings were not suitable to represent benchmark conditions. One site lacked suitable quality habitat or sufficient nutrients to support a healthy population of invertebrates, causing low measures of diversity. The other site appeared to be affected by sedimentation and low flows.</p>\n<p>The classification groupings did not show any significant relations to percentage agricultural land use. Percentage of agricultural land use varied greatly within each group and the means for each group were similar. All streams in this study had some level of protection from agricultural practices in their basins. Although the intensity of agriculture is known to be a factor causing deterioration of invertebrate populations in past studies, the finding in this study indicated that the level of protection the stream received and other factors such as environmental setting and habitat could be more important to benthic invertebrates than the percentage of agriculture in the basin.</p>\n<p>Information gathered from these benchmark streams can be used as a regional reference for comparison with other streams in agricultural areas, based on communities of aquatic biota, habitat, and water quality.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964038C","usgsCitation":"Rheaume, S.J., Lenz, B.N., and Scudder, B.C., 1996, Benthic invertebrates of benchmark streams in agricultural areas of eastern Wisconsin — Western Lake Michigan drainages: U.S. Geological Survey Water-Resources Investigations Report 96-4038, vi, 39 p., https://doi.org/10.3133/wri964038C.","productDescription":"vi, 39 p.","numberOfPages":"46","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":394722,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48405.htm"},{"id":58180,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4038c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":119051,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4038c/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","otherGeospatial":"Lake Michigan","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -89.483642578125,\n              43.1090040242731\n            ],\n            [\n              -89.483642578125,\n              45.46783598133375\n            ],\n            [\n              -86.737060546875,\n              45.46783598133375\n            ],\n            [\n              -86.737060546875,\n              43.1090040242731\n            ],\n            [\n              -89.483642578125,\n              43.1090040242731\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a53e4b07f02db62b4bb","contributors":{"authors":[{"text":"Rheaume, S. J.","contributorId":70804,"corporation":false,"usgs":true,"family":"Rheaume","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":201366,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lenz, B. N.","contributorId":106164,"corporation":false,"usgs":true,"family":"Lenz","given":"B.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":201368,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Scudder, B. C.","contributorId":71588,"corporation":false,"usgs":true,"family":"Scudder","given":"B.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":201367,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":26669,"text":"wri954278 - 1996 - Influences of environmental settings on aquatic ecosystems in the Apalachicola-Chattahoochee-Flint River basin","interactions":[],"lastModifiedDate":"2023-01-11T21:49:05.716986","indexId":"wri954278","displayToPublicDate":"1997-07-01T00:00:00","publicationYear":"1996","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":"95-4278","title":"Influences of environmental settings on aquatic ecosystems in the Apalachicola-Chattahoochee-Flint River basin","docAbstract":"<p>The watershed boundary of the Apalachicola-Chattahoochee-Flint (ACF) River basin defines an aquatic ecosystem whose water quality is the result of complex interactions of natural and human influences on land and water resources. Topics relating to the basin's environmental setting-its physical, biological, and cultural characteristics-are summarized to provide an understanding of factors that influence water quality and the health of aquatic ecosystems.</p><p>The ACF River basin lies partly in southwestern Georgia, southeastern Alabama, and northwestern Florida and covers 19,800 square miles in the Blue Ridge, the Piedmont, and the Coastal Plain Provinces. The basin includes the drainages of the Chattahoochee River and the Flint River, which meet to form the Apalachicola River. The Apalachicola River flows into the Gulf of Mexico at Apalachicola Bay. Basin hydrology and water quality are influenced by 16 mainstem reservoirs, 13 of which are on the Chattahoochee River. Ground water in the basin is contained in six aquifers-the surficial aquifer system, the Floridan aquifer system, the Claiborne aquifer, the Clayton aquifer, the Providence aquifer, and the crystalline-rock aquifer.</p><p>Physiography, climate, and hydrology of the ACF River basin provide natural conditions that support a rich and abundant diversity of plants and animals. Although most of the ACF River basin has been altered by human activities, the basin's environment is noteworthy for its remaining biological diversity and the role it plays in sustaining biological productivity in Apalachicola Bay. The Bay produces 90 percent of Florida's and 13 percent of the Nation's oyster harvest; and functions as a nursery for penaeid shrimp, blue crabs, and a variety of fin fish. The diversity of the basin's aquatic fauna is noteworthy because the basin is home to (1) the largest number of fish species among Gulf Coast drainages east of the Mississippi River, (2) the largest assemblage of freshwater fish in Florida, (3) the largest number of mollusc species among western Florida drainages, and (4) the highest species density of amphibians and reptiles on the continent north of Mexico.</p><p>Population of the ACF River basin in 1990 was estimated at 2.6 million. Nearly 90 percent of the total population lived in Georgia, and nearly 60 percent lived in the Metropolitan Atlanta area. The 1990 basin population is projected to increase by 15 percent to 3.0 million by the year 2000, and by 30 percent to 3.4 million by 2010. The largest increases in populations are projected for the Metropolitan Atlanta area.</p><p>In 1972-76, approximately 59 percent of the basin was covered by forest, 29 percent was agricultural, 5 percent was wetland, 4 percent was urban, and 3 percent was water or barren land. Most of the original land cover of the basin has been transformed by human activity. Timber is the basin's largest cash crop and most forests consist of second-growth stands or large acreages of planted pine. The dominant agricultural land use in the Piedmont Province is pasture and confined feeding for dairy, livestock, and poultry production. Row-crop agriculture, orchards, and silviculture are most common in the Coastal Plain Province. The top five crops in order from most to least acres harvested in 1990 were peanuts, corn, soybeans, wheat, and cotton.</p><p>The water in the basin is used for public and industrial supply, irrigation, power generation, navigation, and recreation. Although most public-supply withdrawals in the Blue Ridge and Piedmont Provinces are from surface-water sources, with the exception of counties near or immediately below the Fall Line, all publicly supplied water in the Coastal Plain is withdrawn from ground-water sources. Ground water supplied 18 percent of the basin's population served by public supply. Total water withdrawn in the ACF River basin in 1990 was 2,098 million gallons per day (Mgal/d), of which Georgia withdrew 82 percent and Florida and Alabama each withdrew 9 percent. Power generation is the single largest water use. Sixteen of the basin's 22 power generating plants are located along the mainstem of the Chattahoochee River. The U.S. Army Corps of Engineers maintains a navigation channel from the mouth of the Apalachicola River to Columbus, Ga., on the Chattahoochee River and to Bainbridge, Ga., on the Flint River.</p><p>Water quality in the basin is influenced by the operation of 137 municipal wastewater-treatment facilities. In 1990, 354 Mgal/d of municipal wastewater was discharged within the ACF River basin. Eighty-eight percent of the wastewater was discharged into the Chattahoochee River basin, 10.6 percent into the Flint River basin, and 1.4 percent into the Apalachicola River basin.</p><p>Two-thirds of the 938 stream miles in the Georgia portion of the ACF River basin having water quality that does not meet or only partially meets the designated-use criteria in the Chattahoochee River basin. The Chattahoochee River is the most heavily-used water resource both in the ACF River basin and in Georgia. Urban runoff or unknown nonpoint sources are cited as the causes of water-quality regulations in 72 percent of violations. The remaining causes primarily are combined sewer overflows in the Atlanta area, and discharges from municipal or industrial treatment facilities with inadequate treatment capabilities or operational deficiencies.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954278","usgsCitation":"Couch, C.A., Hopkins, E.H., and Hardy, P.S., 1996, Influences of environmental settings on aquatic ecosystems in the Apalachicola-Chattahoochee-Flint River basin: U.S. Geological Survey Water-Resources Investigations Report 95-4278, v, 58 p., https://doi.org/10.3133/wri954278.","productDescription":"v, 58 p.","costCenters":[],"links":[{"id":411748,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48352.htm","linkFileType":{"id":5,"text":"html"}},{"id":55537,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4278/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":13458,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/wri/wrir95-4278/","linkFileType":{"id":5,"text":"html"}},{"id":119083,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4278/report-thumb.jpg"}],"country":"United States","state":"Alabama, Florida, Georgia","otherGeospatial":"Apalachicola-Chattahoochee-Flint River basin","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -85.45,\n              34.8333\n            ],\n            [\n              -85.45,\n              29.6267\n            ],\n            [\n              -83.5167,\n              29.6267\n            ],\n            [\n              -83.5167,\n              34.8333\n            ],\n            [\n              -85.45,\n              34.8333\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f1e4b07f02db5ee565","contributors":{"authors":[{"text":"Couch, C. A.","contributorId":36972,"corporation":false,"usgs":true,"family":"Couch","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":196802,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hopkins, E. H.","contributorId":18411,"corporation":false,"usgs":true,"family":"Hopkins","given":"E.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":196801,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hardy, P. S.","contributorId":16461,"corporation":false,"usgs":true,"family":"Hardy","given":"P.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":196800,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":6227,"text":"pp1412A - 1996 - Summary of the Oahu, Hawaii, regional aquifer-system analysis","interactions":[],"lastModifiedDate":"2025-05-22T17:50:31.462503","indexId":"pp1412A","displayToPublicDate":"1997-06-01T00:00:00","publicationYear":"1996","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":"1412","chapter":"A","title":"Summary of the Oahu, Hawaii, regional aquifer-system analysis","docAbstract":"Oahu, the third largest of the Hawaiian islands, is formed by the eroded remnants of two elongated shield volcanoes with broad, low profiles. Weathering and erosion have modified the original domed surfaces of the volcanoes, leaving a landscape of deep valleys and steep interfluvial ridges in the interior highlands. The Koolau Range in eastern Oahu and the Waianae Range in western Oahu are the eroded remnants of the Koolau and Waianae Volcanoes.\r\n\r\nThe origin, mode of emplacement, texture, and composition of the rocks of Oahu affect their ability to store and transmit water. The volcanic rocks are divided into four groups: (1) lava flows, (2) dikes, (3) pyroclastic deposits, and (4) saprolite and weathered basalt. Stratified sequences of thin-bedded lava flows form the most productive aquifers in Hawaii. Dikes are near-vertical sheets of massive intrusive rock that typically contain only fracture permeability. Pyroclastic deposits include ash, cinder, and spatter; they are essentially granular, with porosity and permeability similar to those of granular sediments. Weathering of basaltic rocks in the humid, subtropical climate of Oahu alters igneous minerals to clays and oxides, reducing the permeability of the parent rock. Saprolite is weathered material that has retained textural features of the parent rock.\r\n\r\nEstimates of hydraulic conductivity along the plane of dike-free lava flows tend to fall within about one order of magnitude, from about 500 to about 5,000 feet per day. Estimates of specific yield range from about 1 to 20 percent; most of the values lie within a narrow range of about 5 to 10 percent.\r\n\r\nThe occurrence of ground water on Oahu is determined by the type and character of the rocks and by the presence of geohydrologic barriers. The primary modes of freshwater occurrence on Oahu are as a basal lens of fresh ground water floating on saltwater, as dike-impounded ground water, and as perched ground water. Saltwater occurs at depth throughout much of the island.\r\n\r\nA regional aquifer system composed of the Waianae aquifer in the Waianae Volcanics and the Koolau aquifer in the Koolau Basalt is subdivided into well-defined areas by geohydrologic barriers. The aquifers are separated by the Waianae confining unit formed by weathering along the Waianae-Koolau unconformity. In some coastal areas, a caprock of sedimentary deposits overlies and confines the aquifers.\r\n\r\nThe island of Oahu has been divided into seven major ground-water areas delineated by deep-seated structural geohydrologic barriers; these areas are further subdivided by shallower internal barriers to ground-water flow. The Koolau rift zone along the eastern (windward) side of the island and the Waianae rift zone to the west (Waianae area) constitute two of the major ground-water areas. North-central Oahu is divided into three smaller ground-water areas, Mokuleia, Waialua, and Kawailoa. The Schofield ground-water area encompasses much of the Schofield Plateau of central Oahu. Southern Oahu is divided into six areas, Ewa, Pearl Harbor, Moanalua, Kalihi, Beretania, and Kaimuki. Southeastern Oahu is divided into the Waialae and Wailupe-Hawaii Kai areas. Along the northeast coast of windward Oahu is the Kahuku ground-water area.\r\n\r\nThe aquifers of Oahu contain shallow freshwater and deeper saltwater flow systems. There are five fresh ground-water flow systems: meteoric freshwater flow diverges from ground-water divides that lie somewhere within the Waianae and Koolau rift zones, forming an interior flow system in central Oahu (which is divided into the northern and southern Oahu flow systems) and exterior flow systems in western (Waianae area) Oahu, eastern (windward) Oahu, and southeastern Oahu.\r\n\r\nDevelopment of the ground-water resources on Oahu began when the first well was drilled near Honouliuli in the summer of 1879. By 1890, 86 wells had been drilled on the island. From about 1891 to about 1910, development increased rapidly with the drilling of a","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1412A","usgsCitation":"Nichols, W., Shade, P.J., and Hunt, C.D., 1996, Summary of the Oahu, Hawaii, regional aquifer-system analysis: U.S. Geological Survey Professional Paper 1412, viii, 71 p. *MISSING PAGES*, https://doi.org/10.3133/pp1412A.","productDescription":"viii, 71 p. *MISSING PAGES*","costCenters":[{"id":525,"text":"Pacific Islands Water Science Center","active":true,"usgs":true}],"links":[{"id":117833,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1412a/report-thumb.jpg"},{"id":94746,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1412a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":486410,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4868.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Oahu","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -158.3019853212155,\n              21.587546117430605\n            ],\n            [\n              -158.12029304901154,\n              21.278411927892975\n            ],\n            [\n              -157.95027578225046,\n              21.273733453894693\n            ],\n            [\n              -157.70437098011104,\n              21.23768539325078\n            ],\n            [\n              -157.61899750281034,\n              21.284611779277185\n            ],\n            [\n              -157.7182350490743,\n              21.48980076150177\n            ],\n            [\n              -157.97800392017717,\n              21.727240606356965\n            ],\n            [\n              -158.3019853212155,\n              21.587546117430605\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db6981c1","contributors":{"authors":[{"text":"Nichols, William D.","contributorId":98296,"corporation":false,"usgs":true,"family":"Nichols","given":"William D.","affiliations":[],"preferred":false,"id":152342,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Shade, Patricia J.","contributorId":30618,"corporation":false,"usgs":true,"family":"Shade","given":"Patricia","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":152341,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hunt, Charles D. 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The assessment, which was conducted by regional assessment teams of scientists from the USGS, was based on the concepts of permissive tracts and deposit models. Permissive tracts are discrete areas of the United States for which estimates of numbers of undiscovered deposits of a particular deposit type were made. A permissive tract is defined by its geographic boundaries such that the probability of deposits of the type delineated occurring outside the boundary is neglible. Deposit models, which are based on a compilation of worldwide literature and on observation, are sets of data in a convenient form that describe a group of deposits which have similar characteristics and that contain information on the common geologic attributes of the deposits and the environments in which they are found. Within each region, the assessment teams delineated permissive tracts for those deposit models that were judged to be appropriate and, when the amount of information warranted, estimated the number of undiscovered deposits. A total of 46 deposit models were used to assess 236 separate permissive tracts. Estimates of undiscovered deposits were limited to a depth of 1 km beneath the surface of the Earth. \r\n\r\nThe estimates of the number of undiscovered deposits of gold, silver, copper, lead, and zinc were expressed in the form of a probability distribution. Commonly, the number of undiscovered deposits was estimated at the 90th, 50th, and 10th percentiles. A Monte Carlo simulation computer program was used to combine the probability distribution of the number of undiscovered deposits with the grade and tonnage data sets associated with each deposit model to obtain the probability distribution for undiscovered metal.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr9696","issn":"0566-8174","usgsCitation":"Ludington, S.D., Cox, D.P., and McCammon, R., 1996, Data base for a national mineral-resource assessment of undiscovered deposits of gold, silver, copper, lead, and zinc in the conterminous United States (Superseded by OFR 2002-198): U.S. Geological Survey Open-File Report 96-96, HTML Document; CD-ROM, https://doi.org/10.3133/ofr9696.","productDescription":"HTML Document; CD-ROM","costCenters":[{"id":595,"text":"U.S. Geological 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D.","contributorId":80682,"corporation":false,"usgs":true,"family":"Ludington","given":"S.","middleInitial":"D.","affiliations":[],"preferred":false,"id":185360,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cox, D. P.","contributorId":82689,"corporation":false,"usgs":true,"family":"Cox","given":"D.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":185361,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McCammon, R.B.","contributorId":17218,"corporation":false,"usgs":true,"family":"McCammon","given":"R.B.","email":"","affiliations":[],"preferred":false,"id":185359,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":24371,"text":"ofr96468 - 1996 - Hydrologic data for wetland sites at Millington, Shelby County, and Huntingdon, Carroll County, Tennessee, May 1994 through September 1995","interactions":[],"lastModifiedDate":"2012-02-02T00:08:11","indexId":"ofr96468","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-468","title":"Hydrologic data for wetland sites at Millington, Shelby County, and Huntingdon, Carroll County, Tennessee, May 1994 through September 1995","docAbstract":"Hydrologic data at two wetland sites near Millington and Huntingdon in West Tennessee were collected to assist efforts by the Tennessee Department of Transportation to determine hydrologic conditions at the sites prior to wetland restoration. The Millington site is located along the Big Creek Drainage Canal east of State Route 240. Water levels were monitored in thirteen 8-inch-diameter wells from July 1994 through September 1995. Water-level recorders provided continuous measurement of water level during periods of wetland inundation and depth to water table during periods of noninundation. A crest-stage indicator and a continuous-stage recorder were installed to monitor surface-water fluctuation. Precipitation data were recorded to determine timing and duration of rainfall events. Land surface at the wells was inundated from 0 to 48 percent of the study period. Additionally, water levels at the wells were within 1.5 feet of the land surface from 0 to 56 percent of the study period. The Huntingdon study site is located along the Crooked Creek Drainage Canal at State Route 22. Ground-water levels were monitored in two wells (wells W-1 and W-2) with continuous water- level recorders from May 1994 through September 1995. Water levels did not rise above land surface at either well during the study. Water levels at wells W-1 and W-2 were within 1.5 feet of the land surface 46 and 50 percent of the study period, respectively. Surface-water stage was monitored at a pond on the mitigation site.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/ofr96468","issn":"0094-9140","usgsCitation":"Robinson, J.A., and Diehl, T., 1996, Hydrologic data for wetland sites at Millington, Shelby County, and Huntingdon, Carroll County, Tennessee, May 1994 through September 1995: U.S. Geological Survey Open-File Report 96-468, iv, 31 p. :ill, maps ;28 cm., https://doi.org/10.3133/ofr96468.","productDescription":"iv, 31 p. :ill, maps ;28 cm.","costCenters":[],"links":[{"id":1721,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/ofr96468","linkFileType":{"id":5,"text":"html"}},{"id":156258,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a1ce4b07f02db607c31","contributors":{"authors":[{"text":"Robinson, J. A.","contributorId":57417,"corporation":false,"usgs":true,"family":"Robinson","given":"J.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":191797,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Diehl, T.H.","contributorId":89170,"corporation":false,"usgs":true,"family":"Diehl","given":"T.H.","email":"","affiliations":[],"preferred":false,"id":191798,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":25576,"text":"wri964091 - 1996 - Hydrogeology at Air Force Plant 4 and vicinity and water quality of the Paluxy Aquifer, Fort Worth, Texas","interactions":[],"lastModifiedDate":"2016-08-22T10:57:14","indexId":"wri964091","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4091","title":"Hydrogeology at Air Force Plant 4 and vicinity and water quality of the Paluxy Aquifer, Fort Worth, Texas","docAbstract":"<p>Ground water in the surficial terrace alluvial aquifer is contaminated at Air Force Plant 4, Fort Worth, Texas, and at the adjacent Naval Air Station. Some of the contaminated water has leaked from the terrace alluvial aquifer to an uppermost interval of the Paluxy Formation (the Paluxy \"upper sand\") beneath the east parking lot, east of the assembly building, and to the upper and middle zones of the Paluxy aquifer near Bomber Road, west of the assembly building. Citizens are concerned that contaminants from the plant, principally trichloroethylene and chromium might enter nearby municipal and domestic wells that pump water from the middle and lower zones of the Paluxy aquifer. </p><p>Geologic formations that crop out in the study area, from oldest to youngest, are the Paluxy Formation (aquifer), Walnut Formation (confining unit), and Goodland Limestone (confining unit). Beneath the Paluxy Formation is the Glen Rose Formation (confining unit) and Twin Mountains Formation (aquifer). The terrace alluvial deposits overlie these Cretaceous rocks. </p><p>The terrace alluvial aquifer, which is not used for municipal water supply, is separated from the Paluxy aquifer by the Goodland-Walnut confining unit. The confining unit restricts the flow of ground water between these aquifers in most places; however, downward leakage to the Paluxy aquifer might occur through the \"window,\" where the confining unit is thin or absent. </p><p>The Paluxy aquifer is divided into upper, middle, and lower zones. The Paluxy \"upper sand\" underlying the \"window\" is an apparently isolated, mostly unsaturated, sandy lens within the uppermost part of the upper zone. The Paluxy aquifer is recharged by leakage from Lake Worth and by precipitation on the outcrop area. Discharge from the aquifer primarily occurs as pumpage from municipal and domestic wells. The Paluxy aquifer is separated from the underlying Twin Mountains aquifer by the Glen Rose confining unit. </p><p>Water-level maps indicate that (1) ground water in the terrace alluvial aquifer appears to flow outward, away from Air Force Plant 4; (2) a ground-water mound, possibly caused by downward leakage from the terrace alluvial aquifer, is present in the Paluxy \"upper sand\" beneath the \"window;\" and (3) lateral ground-water flow in regionally extensive parts of the Paluxy aquifer is from west to east-southeast. </p><p>Trichloroethylene concentrations at Air Force Plant 4 have ranged from about 10,000 to about 100,000 micrograms per liter in the terrace alluvial aquifer, from 8,000 to 11,000 micrograms per liter in the Paluxy \"upper sand,\" and from 2 to 50 micrograms per liter in the upper and middle zones of the Paluxy aquifer. Chromium concentrations at Air Force Plant 4 have ranged from 0 to 629 micrograms per liter in the terrace alluvial aquifer. </p><p>The seven municipal wells mostly west and south of Air Force Plant 4 are not along a flowpath for leakage of contaminants from the plant because ground-water flow in the Paluxy aquifer is toward the east-southeast. Furthermore, trichloroethylene was not detected in any of these wells in 1993 when all were sampled for water quality. </p><p>The results of water-quality sampling at 10 domestic wells northwest of the Air Force Plant 4 during April 1993 and April 1995 indicated that neither trichloroethylene nor chromium had migrated off-site to these wells.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Austin, TX","doi":"10.3133/wri964091","collaboration":"Prepared in cooperation with the U.S. Air Force Aeronautical Systems Center, Environmental Management Directorate","usgsCitation":"Kuniansky, E.L., Jones, S.A., Brock, R.D., and Williams, M., 1996, Hydrogeology at Air Force Plant 4 and vicinity and water quality of the Paluxy Aquifer, Fort Worth, Texas: U.S. Geological Survey Water-Resources Investigations Report 96-4091, iv, 41 p., https://doi.org/10.3133/wri964091.","productDescription":"iv, 41 p.","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":1920,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri96-4091/","linkFileType":{"id":5,"text":"html"}},{"id":125023,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/wri_96_4091.jpg"}],"country":"United States","state":"Texas","city":"Fort Worth","otherGeospatial":"Air Force Plant 4","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -97.4625,\n              32.791667\n            ],\n            [\n              -97.4625,\n              32.75\n            ],\n            [\n              -97.416667,\n              32.75\n            ],\n            [\n              -97.416667,\n              32.791667\n            ],\n            [\n              -97.4625,\n              32.791667\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ee4b07f02db6aa6bc","contributors":{"authors":[{"text":"Kuniansky, Eve L. 0000-0002-5581-0225 elkunian@usgs.gov","orcid":"https://orcid.org/0000-0002-5581-0225","contributorId":932,"corporation":false,"usgs":true,"family":"Kuniansky","given":"Eve","email":"elkunian@usgs.gov","middleInitial":"L.","affiliations":[{"id":509,"text":"Office of the Associate Director for Water","active":true,"usgs":true},{"id":5064,"text":"Southeast Regional Director's Office","active":true,"usgs":true}],"preferred":true,"id":194258,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jones, Sonya A. 0000-0002-7462-8576 sajones@usgs.gov","orcid":"https://orcid.org/0000-0002-7462-8576","contributorId":1690,"corporation":false,"usgs":true,"family":"Jones","given":"Sonya","email":"sajones@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":194259,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brock, Robert D.","contributorId":27875,"corporation":false,"usgs":true,"family":"Brock","given":"Robert","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":194260,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Williams, M.D.","contributorId":79507,"corporation":false,"usgs":true,"family":"Williams","given":"M.D.","email":"","affiliations":[],"preferred":false,"id":194261,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":26739,"text":"wri964220 - 1996 - Ground-water recharge to the regolith-fractured crystalline rock aquifer system, Orange County, North Carolina","interactions":[],"lastModifiedDate":"2017-01-27T13:46:42","indexId":"wri964220","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4220","title":"Ground-water recharge to the regolith-fractured crystalline rock aquifer system, Orange County, North Carolina","docAbstract":"Quantitative information concerning recharge rates to aquifers and ground water in storage is needed to manage the development of ground-water resources. The amount of ground water available from the regolith-fractured crystalline rock aquifer system in Orange County, North Carolina, is largely unknown. If historical patterns seen throughout the Piedmont continue into the future, the number of ground-water users in the county can be expected to increase. In order to determine the maximum population that can be supplied by ground water, planners and managers of suburban development must know the amount of ground water that can be withdrawn without exceeding recharge and(or) overdrafting water in long-term storage. Results of the study described in this report help provide this information. Estimates of seasonal and long-term recharge rates were estimated for 12 selected drainage basins and subbasins using streamflow data and an analytical technique known as hydrograph separation. Methods for determining the quality of ground water in storage also are described. \r\n\r\nOrange County covers approximately 401 square miles in the eastern part of the Piedmont Province. The population of the county in 1990 was about 93,850; approximately 41 percent of the population depends on ground water as a source of potable supplies. Ground water is obtained from wells tapping the regolith-fractured crystalline rock aquifer system that underlies most of the county. Ground water also is obtained from Triassic age sedimentary rocks that occur in a small area in southeastern Orange County. \r\n\r\nUnder natural conditions, recharge to the county's ground-water system is derived from the infiltration of precipitation. Ground-water recharge from precipitation cannot be measured directly; however, an estimate of the amount of precipitation that infiltrates into the ground and ultimately reaches the streams of the region can be determined by the technique of hydrograph separation. Data from 17 gaging stations that measure streamflow within or from Orange County were analyzed to produce daily estimates of ground-water recharge in 12 drainage basins and subbasins in the county. The recharge estimates were further analyzed to determine seasonal and long-term recharge rates, as well as recharge duration statistics. \r\n\r\nMean annual recharge in the 12 basins and subbasins ranges from 4.15 to 6.40 inches per year, with a mean value of 4.90 inches per year for all basins. In general, recharge rates are highest for basins along a north- south zone extending down the center of the county, and lowest in the western and southeastern parts of the county. Median recharge rates in the 12 basins range from 1.08 inches per year (80.7 gallons per day per acre) to 4.97 inches per year (370 gallons per day per acre), with a median value of 3.06 inches per year (228 gallons per day per acre) for all basins. \r\n\r\nRecharge estimates for the Morgan Creek Basin upstream from White Cross and upstream from Chapel Hill are higher than any other basin or subbasin in Orange County. Ground water also constitutes a higher percentage of total streamflow in Morgan Creek (44.4 percent upstream from White Cross; 47.9 percent upstream from Chapel Hill) than in any other stream in the county. Greater topographic relief and depth of channel incision may explain the high recharge estimates (base-flow rates) in the Morgan Creek Basin. The presence of large areas of regolith derived from the metaigneous, felsic hydrogeologic unit may magnify the effects of topographic relief and channel incision. Base flow in the New Hope River subbasin, as a percentage of total streamflow, at 32.2 percent, is the lowest of the 12 basins and subbasins. Much of the New Hope River subbasin is underlain by the Triassic sedimentary rock hydrogeologic unit that occurs within a rift basin of Triassic age. These data suggest that in areas underlain by Triassic sedimentary rock, there is less recharge to the ground-water syst","language":"ENGLISH","doi":"10.3133/wri964220","usgsCitation":"Daniel, C.C., 1996, Ground-water recharge to the regolith-fractured crystalline rock aquifer system, Orange County, North Carolina: U.S. Geological Survey Water-Resources Investigations Report 96-4220, vi, 59 p. :ill. ;28 cm., https://doi.org/10.3133/wri964220.","productDescription":"vi, 59 p. :ill. ;28 cm.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":118696,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4220/report-thumb.jpg"},{"id":55618,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4220/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","county":"Orange County","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -83.71307373046874,\n              35.67068501330236\n            ],\n            [\n              -83.71307373046874,\n              35.67068501330236\n            ],\n            [\n              -83.7103271484375,\n              35.67068501330236\n            ],\n            [\n              -83.7103271484375,\n              35.67068501330236\n            ],\n            [\n              -83.71307373046874,\n              35.67068501330236\n            ]\n          ]\n        ]\n      }\n    },\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -79.60693359375,\n              34.867904962568716\n            ],\n            [\n              -79.60693359375,\n              36.43896124085945\n            ],\n            [\n              -77.9150390625,\n              36.43896124085945\n            ],\n            [\n              -77.9150390625,\n              34.867904962568716\n            ],\n            [\n              -79.60693359375,\n              34.867904962568716\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db66711d","contributors":{"authors":[{"text":"Daniel, C. C. III","contributorId":71953,"corporation":false,"usgs":true,"family":"Daniel","given":"C.","suffix":"III","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":196917,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":25842,"text":"wri964192 - 1996 - Water-quality assessment of the White River Basin, Indiana: Analysis of selected information on nutrients, 1980-92","interactions":[],"lastModifiedDate":"2016-06-06T09:21:38","indexId":"wri964192","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4192","title":"Water-quality assessment of the White River Basin, Indiana: Analysis of selected information on nutrients, 1980-92","docAbstract":"<p>Water-quality data from 23 surfacewater-quality monitoring sites operated by the Indiana Department of Environmental Management and streamflow data from 11 U.S. Geological Survey streamflow-gaging stations in the White River Basin were analyzed to determine recent (1981 90 water years) water-quality conditions, trends, and river loads for ammonia, nitrate, total nitrogen, and total phosphorus. The White River Basin drains 11,349 square miles of central and south-central Indiana and is divided into two nearly equal subbasins the East Fork White River and the White River upstream from its confluence with the East Fork (called the \"west fork\" of the White River by the State's water-management agencies).</p>\n<p>Nutrient concentrations generally were higher in the more urbanized west fork than in the more rural east fork because of the much larger volumes of treated municipal sewage, combined-sewer overflows, and urban runoff discharged to the west fork. Concentrations of nutrients, especially ammonia and total phosphorus, were higher downstream from Muncie, Anderson, and Indianapolis than they were upstream from these cities. Nutrient concentrations decreased downstream from Indianapolis in the White River and in the downstream reach of the East Fork White River because of dilution, nitrification, adsorption to stream-bottom sediments, and uptake by aquatic vegetation.</p>\n<p>Seasonal variations in nutrient concentrations and the relations of nutrient concentrations to streamflow depended on the relative contributions of point and nonpoint sources of the nutrients. Total phosphorus increased with increasing streamflow at monitoring sites on the east fork but decreased with increasing streamflow at sites on the west fork. Increasing concentrations of phosphorus with increasing streamflow were consistent with nonpoint sources of phosphorus that wash off land surfaces, whereas decreasing concentrations of phosphorus with increasing streamflow were consistent with dilution of point sources of phosphorus. Median concentrations of total phosphorus were highest during summer and fall downstream from urban areas on the White River because streamflows that dilute point sources of phosphorus are lowest during summer and fall. Median concentrations of ammonia in the White River were highest in winter because of reduced biological uptake and nitrification of ammonia during cold temperatures.</p>\n<p>&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Indianapolis, IN","doi":"10.3133/wri964192","usgsCitation":"Martin, J.D., Crawford, C.G., Frey, J.W., and Hodgkins, G.A., 1996, Water-quality assessment of the White River Basin, Indiana: Analysis of selected information on nutrients, 1980-92: U.S. Geological Survey Water-Resources Investigations Report 96-4192, viii, 91 p., https://doi.org/10.3133/wri964192.","productDescription":"viii, 91 p.","startPage":"1","endPage":"91","numberOfPages":"99","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true},{"id":451,"text":"National Water Quality Assessment 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Center","active":true,"usgs":true}],"preferred":true,"id":195308,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crawford, Charles G. 0000-0003-1653-7841 cgcrawfo@usgs.gov","orcid":"https://orcid.org/0000-0003-1653-7841","contributorId":1064,"corporation":false,"usgs":true,"family":"Crawford","given":"Charles","email":"cgcrawfo@usgs.gov","middleInitial":"G.","affiliations":[{"id":451,"text":"National Water Quality Assessment Program","active":true,"usgs":true},{"id":37947,"text":"Upper Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195306,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Frey, Jeffrey W. 0000-0002-3453-5009 jwfrey@usgs.gov","orcid":"https://orcid.org/0000-0002-3453-5009","contributorId":487,"corporation":false,"usgs":true,"family":"Frey","given":"Jeffrey","email":"jwfrey@usgs.gov","middleInitial":"W.","affiliations":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true},{"id":27231,"text":"Indiana-Kentucky Water Science Center","active":true,"usgs":true},{"id":35860,"text":"Ohio-Kentucky-Indiana Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195309,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Hodgkins, Glenn A. 0000-0002-4916-5565 gahodgki@usgs.gov","orcid":"https://orcid.org/0000-0002-4916-5565","contributorId":2020,"corporation":false,"usgs":true,"family":"Hodgkins","given":"Glenn","email":"gahodgki@usgs.gov","middleInitial":"A.","affiliations":[{"id":371,"text":"Maine Water Science Center","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":195307,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":30532,"text":"wri964122 - 1996 - Use of dye tracing in water-resources investigations in Wyoming, 1967-94","interactions":[],"lastModifiedDate":"2012-02-02T00:09:12","indexId":"wri964122","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4122","title":"Use of dye tracing in water-resources investigations in Wyoming, 1967-94","docAbstract":"During 1967-94, the U.S. Geological Survey made numerous applications of dye tracing for water-resources investigations in Wyoming. Many of the dye tests were done in cooperation with other agencies. Results of all applications, including some previously unpublished, are described. A chronology of past applications in Wyoming and a discussion of potential future applications are included. Time-of-travel and dispersion measurements were made in a 113-mile reach of the Wind/Bighorn River below Boysen Dam; a 117-mile reach of the Green River upstream from Fontenelle Reservoir and a 70-mile reach downstream; parts of four tributaries to the Green (East Fork River, 39 miles; Big Sandy River, 112 miles; Horse Creek, 14 miles; and Blacks Fork, 14 miles); a 75-mile reach of the Little Snake River along the Wyoming-Colorado State line; and a 95-mile reach of the North Platte River downstream from Casper. Reaeration measurements were made during one of the time-of-travel measurements in the North Platte River. Sixty-eight dye-dilution measurements of stream discharge were made at 22 different sites. These included 17 measurements for verifying the stage-discharge relations for streamflow-gaging stations on North and South Brush Creeks near Saratoga, and total of 29 discharge measurements at 12 new stations at remote sites on steep, rough mountain streams crossing limestone outcrops in northeastern Wyoming. The largest discharge measured by dye tracing was 2,300 cubic feet per second. In karst terrane, four losing streams-North Fork Powder River, North Fork Crazy Woman Creek, Little Tongue River, and Smith Creek-were dye-tested. In the Middle Popo Agie River, a sinking stream in Sinks Canyon State Park, a dye test verified the connection of the sink (Sinks of Lander Cave) to the rise, where flow in the stream resumes.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBranch of Information Services [distributor],","doi":"10.3133/wri964122","usgsCitation":"Wilson, J.F., and Rankl, J., 1996, Use of dye tracing in water-resources investigations in Wyoming, 1967-94: U.S. Geological Survey Water-Resources Investigations Report 96-4122, vi, 64 p. :ill, maps ;28 cm., https://doi.org/10.3133/wri964122.","productDescription":"vi, 64 p. :ill, maps ;28 cm.","costCenters":[],"links":[{"id":161208,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4122/report-thumb.jpg"},{"id":59309,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4122/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e487ee4b07f02db514c07","contributors":{"authors":[{"text":"Wilson, J. F. Jr.","contributorId":99541,"corporation":false,"usgs":true,"family":"Wilson","given":"J.","suffix":"Jr.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":203413,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rankl, J.G.","contributorId":107733,"corporation":false,"usgs":true,"family":"Rankl","given":"J.G.","affiliations":[],"preferred":false,"id":203414,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":26901,"text":"wri964218 - 1996 - Hydraulic conductivity of the streambed, east branch Grand Calumet River, northern Lake County, Indiana","interactions":[],"lastModifiedDate":"2016-05-16T07:57:41","indexId":"wri964218","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4218","title":"Hydraulic conductivity of the streambed, east branch Grand Calumet River, northern Lake County, Indiana","docAbstract":"<p>Horizontal and vertical hydraulic conductivity of the Streambed were estimated from results of hydraulic tests along four transects across the east branch Grand Calumet River in northern Lake County, Indiana. Tests were done in two types of temporary wells installed in the Streambed 2-inch-diameter wells that had a 1- or 2-foot length of wire-wrapped screen and 3-inch-diameter wells that were open at the ends. When possible, the hydraulic tests included monitoring both falling- and rising-water levels. A total of 47 tests for horizontal hydraulic conductivity and 20 tests for vertical hydraulic conductivity were done.</p>\n<p>Data collected during the tests were analyzed by use of methods developed by earlier investigators. Horizontal hydraulic conductivity of the streambed was varied and ranged from 1.Ox1O<sup>-2</sup> to 1.2x1O<sup>+3</sup> feet per day. Compared to the previously reported range of horizontal hydraulic conductivity for the Calumet aquifer, 6.5X10<sup>-1</sup> to 3.6x1O<sup>+2</sup> feet per day, results of 24 hydraulic tests in the streambed of the east branch Grand Calumet River were within the reported range, 18 were less than the lowest reported value, and 5 were greater than the highest reported value.</p>\n<p>Vertical hydraulic conductivity of the streambed was less varied than horizontal hydraulic conductivity and ranged from 3.Ox1O<sup>-1</sup> to 7.3x1O<sup>+1</sup> feet per day. The ratio between horizontal and vertical hydraulic conductivity calculated for each transect ranged from 1:0.09 to 1:8.5.</p>\n<p>The hydraulic conductivity of the streambed generally was dependant on the type of sediments in the part of the streambed that was tested. Although most of the streambed contained soft, fine-grained sediments, parts of the streambed also contained fill materials including coal, cinders, and concrete and asphalt rubble. The highest values of horizontal hydraulic conductivity generally were calculated from data collected at locations where the streambed contained fill materials, particularly concrete and asphalt rubble. Horizontal hydraulic conductivities determined for 11 hydraulic tests in predominantly fill materials ranged from 1.2x1O<sup>+1</sup> to 1.2x1O<sup>+3</sup> feet per day and averaged 5.6x1O<sup>+2</sup> feet per day. The lowest values of horizontal hydraulic conductivity were calculated from data collected at locations where the streambed contained fine-grained sediments. Horizontal hydraulic conductivities determined for 36 hydraulic tests in predominantly fine-grained sediments ranged from 1.Ox1O<sup>-2</sup> to 2.4x1O<sup>+2</sup> feet per day and averaged 1.5x1O<sup>+1</sup> feet per day.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964218","collaboration":"Indiana Department of Environmental Management","usgsCitation":"Duwelius, R., 1996, Hydraulic conductivity of the streambed, east branch Grand Calumet River, northern Lake County, Indiana: U.S. Geological Survey Water-Resources Investigations Report 96-4218, v, 37 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri964218.","productDescription":"v, 37 p. :ill., maps ;28 cm.","startPage":"1","endPage":"37","numberOfPages":"41","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":125111,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4218/report-thumb.jpg"},{"id":55782,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4218/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Indiana","county":"Lake","otherGeospatial":"Grand Calumet River","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-87.2223,41.6248],[-87.2222,41.6152],[-87.2221,41.6039],[-87.2218,41.5698],[-87.22,41.4632],[-87.2198,41.3747],[-87.2196,41.3601],[-87.22,41.3388],[-87.2198,41.3188],[-87.2197,41.3043],[-87.2189,41.2893],[-87.2187,41.2744],[-87.2193,41.2671],[-87.219,41.2426],[-87.2184,41.2417],[-87.2263,41.2353],[-87.2762,41.2187],[-87.2859,41.2154],[-87.3241,41.1862],[-87.3313,41.1829],[-87.3405,41.1824],[-87.3448,41.1824],[-87.38,41.1726],[-87.394,41.1625],[-87.4,41.1625],[-87.4055,41.1625],[-87.4147,41.1619],[-87.4411,41.1731],[-87.4466,41.174],[-87.4484,41.1744],[-87.4587,41.1702],[-87.4801,41.1701],[-87.5263,41.1661],[-87.5261,41.267],[-87.5265,41.2983],[-87.527,41.4086],[-87.5265,41.4712],[-87.5255,41.5516],[-87.5239,41.6941],[-87.524,41.7135],[-87.5234,41.7131],[-87.5134,41.7054],[-87.5158,41.7027],[-87.5133,41.7004],[-87.4997,41.6914],[-87.4922,41.6865],[-87.4848,41.6843],[-87.4829,41.6811],[-87.4768,41.6789],[-87.4712,41.6753],[-87.4613,41.6718],[-87.4503,41.6741],[-87.4397,41.6647],[-87.436,41.6656],[-87.4355,41.6729],[-87.4245,41.6802],[-87.4177,41.6753],[-87.4396,41.6565],[-87.4228,41.6439],[-87.4167,41.6439],[-87.4099,41.644],[-87.4087,41.644],[-87.4044,41.6413],[-87.392,41.6382],[-87.3748,41.6329],[-87.3711,41.6315],[-87.3538,41.6285],[-87.3384,41.6259],[-87.3274,41.6259],[-87.3218,41.6219],[-87.315,41.6201],[-87.3101,41.6201],[-87.3058,41.6202],[-87.3003,41.6202],[-87.296,41.6198],[-87.2831,41.6203],[-87.2702,41.6208],[-87.2223,41.6248]]]},\"properties\":{\"name\":\"Lake\",\"state\":\"IN\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cfe4b07f02db54629e","contributors":{"authors":[{"text":"Duwelius, R.F.","contributorId":28250,"corporation":false,"usgs":true,"family":"Duwelius","given":"R.F.","affiliations":[],"preferred":false,"id":197217,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":26144,"text":"wri964209 - 1996 - Hydrogeology and water quality of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren site, Dahlgren, Virginia","interactions":[],"lastModifiedDate":"2023-04-13T19:58:23.68834","indexId":"wri964209","displayToPublicDate":"1997-05-01T00:00:00","publicationYear":"1996","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":"96-4209","title":"Hydrogeology and water quality of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren site, Dahlgren, Virginia","docAbstract":"<p>In October 1993, the U.S. Geological Survey began a study to characterize the hydrogeology of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren Site, Dahlgren, Virginia, which is located on the Potomac River in the Coastal Plain Physiographic Province. The study provides a description of the hydrogeologic units, directions of ground-water flow, and back-ground water quality in the study area to a depth of about 100 feet. Lithologic, geophysical, and hydrologic data were collected from 28 wells drilled for this study, from 3 existing wells, and from outcrops. </p><p>The shallow aquifer system at the Explosive Experimental Area consists of two fining-upward sequences of Pleistocene fluvial-estuarine deposits that overlie Paleocene-Eocene marine deposits of the Nanjemoy-Marlboro confining unit. The surficial hydrogeologic unit is the Columbia aquifer. Horizontal linear flow of water in this aquifer generally responds to the surface topography, discharging to tidal creeks, marshes, and the Potomac River, and rates of flow in this aquifer range from 0.003 to 0.70 foot per day. </p><p>The Columbia aquifer unconformably overlies the upper confining unit 12-an organic-rich clay that is 0 to 55 feet thick. The upper confining unit conformably overlies the upper confined aquifer, a 0- to 35-feet thick unit that consists of interbedded fine-grained to medium-grained sands and clay. The upper confined aquifer probably receives most of its recharge from the adjacent and underlying Nanjemoy-Marlboro confining unit. Water in the upper confined aquifer generally flows eastward, northward, and northeastward at about 0.03 foot per day toward the Potomac River and Machodoc Creek. </p><p>The Nanjemoy-Marlboro confining unit consists of glauconitic, fossiliferous silty fine-grained sands of the Nanjemoy Formation. Where the upper confined system is absent, the Nanjemoy-Marlboro confining unit is directly overlain by the Columbia aquifer. In some parts of the Explosive Experimental Area, horizontal hydraulic conductivities of the Nanjemoy-Marlboro confining unit and the Columbia aquifer are similar (from 10<sup>-4</sup> to 10<sup>-2</sup> foot per day), and these units effectively combine to form a thick (greater than 50 feet) aquifer. </p><p>The background water quality of the shallow aquifer system is characteristic of ground waters in the Virginia Coastal Plain Physiographic Province. Water in the Columbia aquifer is a mixed ionic type, has a median pH of 5.9, and a median total dissolved solids of 106 milligrams per liter. Water in the upper confined aquifer and Nanjemoy-Marlboro confining unit is a sodium- calcium-bicarbonate type, and generally has higher pH, dissolved solids, and alkalinity than water in the Columbia aquifer. Water in the upper confined aquifer and some parts of the Columbia aquifer is anoxic, and it has high concentrations of dissolved iron, manganese, and sulfide.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964209","usgsCitation":"Bell, C.F., 1996, Hydrogeology and water quality of the shallow aquifer system at the Explosive Experimental Area, Naval Surface Warfare Center, Dahlgren site, Dahlgren, Virginia: U.S. Geological Survey Water-Resources Investigations Report 96-4209, v, 37 p., https://doi.org/10.3133/wri964209.","productDescription":"v, 37 p.","costCenters":[],"links":[{"id":54940,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4209/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122911,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4209/report-thumb.jpg"},{"id":415729,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_48543.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Virginia","city":"Dahlgren","otherGeospatial":"Explosive Experimental Area, Naval Surface Warfare Center","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -77.0597,\n              38.3167\n            ],\n            [\n              -77.0597,\n              38.279\n            ],\n            [\n              -77.0167,\n              38.279\n            ],\n            [\n              -77.0167,\n              38.3167\n            ],\n            [\n              -77.0597,\n              38.3167\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db625174","contributors":{"authors":[{"text":"Bell, C. F.","contributorId":14449,"corporation":false,"usgs":true,"family":"Bell","given":"C.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":195893,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":26564,"text":"wri944090 - 1996 - Hydrogeology of, and simulation of ground-water flow in, a mantled carbonate-rock system, Cumberland Valley, Pennsylvania","interactions":[],"lastModifiedDate":"2022-02-03T20:34:37.822011","indexId":"wri944090","displayToPublicDate":"1997-04-01T00:00:00","publicationYear":"1996","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":"94-4090","title":"Hydrogeology of, and simulation of ground-water flow in, a mantled carbonate-rock system, Cumberland Valley, Pennsylvania","docAbstract":"The U.S. Geological Survey conducted a study in a highly productive and complex regolith-mantled carbonate valley in the northeastern part of the Cumberland Valley, Pa., as part of its Appalachian Valleys and Piedmont Regional Aquifer-system Analysis program. The study was designed to quantify the hydrogeologic characteristics and understand the ground-water flow system of a highly productive and complex thickly mantled carbonate valley. The Cumberland Valley is characterized by complexly folded and faulted carbonate bedrock in the valley bottom, by shale and graywacke to the north, and by red-sedimentary and diabase rocks in the east-southeast. Near the southern valley hillslope, the carbonate rock is overlain by wedge-shaped deposit of regolith, up to 450 feet thick, that is composed of residual material, alluvium, and colluvium. Locally, saturated regolith is greater than 200 feet thick. Seepage-run data indicate that stream reaches, near valley walls, are losing water from the stream, through the regolith, to the ground-water system. Results of hydrograph-separation analyses indicate that base flow in stream basins dominated by regolith-mantled carbonate rock, carbonate rock, and carbonate rock and shale are 81.6, 93.0, and 67.7 percent of total streamflow, respectively. The relative high percentage for the regolith-mantled carbonate-rock basin indicates that the regolith stores precipitation and slowly, steadily releases this water to the carbonate-rock aquifer and to streams as base flow. Anomalies in water-table gradients and configuration are a result of topography and differences in the character and distribution of overburden material, permeability, rock type, and geologic structure. Most ground-water flow is local, and ground water discharges to nearby springs and streams. Regional flow is northeastward to the Susquehanna River. Average-annual water budgets were calculated for the period of record from two continuous streamflow-gaging stations. Average-annual precipitation range from 39.0 to 40.5 inches, and averages about 40 inches for the model area. Average-annual recharge, which was assumed equal to the average-annual base flow, ranged from 12 inches for the Conodoguinet Creek, and 15 inches for the Yellow Breeches Creek. The thickly-mantled carbonate system was modeled as a three- dimensional water-table aquifer. Recharge to, ground-water flow through, and discharge from the Cumberland Valley were simulated. The model was calibrated for steady-state conditions using average recharge and discharge data. Aquifer horizontal hydraulic conductivity was calculated from specific-capacity data for each geologic unit in the area. Particle-tracking analyses indicate that interbasin and intrabasin flows of groundwater occur within the Yellow Breeches Creek Basin and between the Yellow Breeches and Conodoguinet Creek Basins.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri944090","usgsCitation":"Chichester, D., 1996, Hydrogeology of, and simulation of ground-water flow in, a mantled carbonate-rock system, Cumberland Valley, Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 94-4090, v, 39 p., https://doi.org/10.3133/wri944090.","productDescription":"v, 39 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":395404,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_47983.htm"},{"id":55429,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1994/4090/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123756,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1994/4090/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Cumberland Valley","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -77.6167,\n              39.95\n            ],\n            [\n              -76.8528,\n              39.95\n            ],\n            [\n              -76.8528,\n              40.333\n            ],\n            [\n              -77.6167,\n              40.333\n            ],\n            [\n              -77.6167,\n              39.95\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2de4b07f02db6148e9","contributors":{"authors":[{"text":"Chichester, D. C.","contributorId":61856,"corporation":false,"usgs":true,"family":"Chichester","given":"D. C.","affiliations":[],"preferred":false,"id":196626,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":30588,"text":"wri954243 - 1996 - Water quality of large discharges from mines in the anthracite region of eastern Pennsylvania","interactions":[],"lastModifiedDate":"2017-06-06T14:23:27","indexId":"wri954243","displayToPublicDate":"1997-04-01T00:00:00","publicationYear":"1996","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":"95-4243","title":"Water quality of large discharges from mines in the anthracite region of eastern Pennsylvania","docAbstract":"In 1991, 99 of the 102 coal mines in the anthracite coal fields of Pennsylvania that discharged 1.0 cubic foot per second or more when water-quality samples were collected in 1975 were revisited. Water was not discharging from 15 of these 99 mines in 1991. Discharge, water temperature, specific conductance, pH, dissolved oxygen, sulfate, iron, manganese, alkalinity, and acidity were measured in water samples collected at 84 mines to assess changes in water quality from 1975 to 1991. The pH increased in water samples of 64 of the 81 mines. However, acidity was essentially unchanged. Concentrations of iron decreased in water discharge samples from 57 of 82 mines, manganese concentrations decreased in samples from 23 of 26 mines, and sulfate concentrations decreased in samples from 62 of 77 mines. The median change in sulfate was a decrease of 139 milligrams per liter. Alkalinity increased in water discharge samples from 43 mines, remained the same at 22 mines, and decreased at 14 mines. In 1975, the samples were collected during high base flow in the spring; in 1991, samples were collected during lower-than-normal base flow in the fall. This may have affected the comparison.\r\n      Many mine discharges have elevated concentrations of aluminum, calcium, cobalt, iron, lithium, magnesium, manganese, nickel, strontium, zinc, and sulfate.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri954243","usgsCitation":"Wood, C.R., 1996, Water quality of large discharges from mines in the anthracite region of eastern Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 95-4243, v, 68 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri954243.","productDescription":"v, 68 p. :ill., maps ;28 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":59348,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1995/4243/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":160299,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1995/4243/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -76.5802001953125,\n              40.30257076364479\n            ],\n            [\n              -75.10528564453125,\n              40.30257076364479\n            ],\n            [\n              -75.10528564453125,\n              41.64623592868676\n            ],\n            [\n              -76.5802001953125,\n              41.64623592868676\n            ],\n            [\n              -76.5802001953125,\n              40.30257076364479\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f9972","contributors":{"authors":[{"text":"Wood, C. R.","contributorId":100386,"corporation":false,"usgs":true,"family":"Wood","given":"C.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":203497,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":4893,"text":"ds41 - 1996 - Great Basin geoscience data base","interactions":[],"lastModifiedDate":"2014-02-28T13:28:18","indexId":"ds41","displayToPublicDate":"1997-04-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":310,"text":"Data Series","code":"DS","onlineIssn":"2327-638X","printIssn":"2327-0271","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"41","title":"Great Basin geoscience data base","docAbstract":"This CD-ROM serves as the archive for 73 digital GIS data set for the Great Basin. The data sets cover Nevada, eastern California, southeastern Oregon, southern Idaho, and western Utah. Some of the data sets are incomplete for the total area. On the CD-ROM, the data are provided in three formats, a prototype Federal Data Exchange standard format, the ESRI PC ARCVIEW1 format for viewing the data, and the ESRI ARC/INFO export format. Extensive documentation is provided to describe the data, the sources, and data enhancements. The following data are provided. One group of coverages comes primarily from 1:2,000,000-scale National Atlas data and can be assembled for use as base maps. These various forms of topographic information. In addition, public land system data sets are provided from the 1:2,500,000-scale Geologic Map of the United States and 1:500,000-scale geologic maps of Nevada, Oregon, and Utah. Geochemical data from the National Uranium Resource Evaluation (NURE) program are provided for most of the Great Basin. Geophysical data are provided for most of the Great Basin, typically gridded data with a spacing of 1 km. The geophysical data sets include aeromagnetics, gravity, radiometric data, and several derivative products. The thematic data sets include geochronology, calderas, pluvial lakes, tectonic extension domains, distribution of pre-Cenozoic terranes, limonite anomalies, Landsat linear features, mineral sites, and Bureau of Land Management exploration and mining permits.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ds41","issn":"1088-1018","isbn":"060786141X","collaboration":"The USGS does not provide technical support for the software associated with this publication.","usgsCitation":"Raines, G.L., Sawatzky, D.L., and Connors, K.A., 1996, Great Basin geoscience data base: U.S. Geological Survey Data Series 41, 1 computer laser optical disc ;4 3/4 in., https://doi.org/10.3133/ds41.","productDescription":"1 computer laser optical disc ;4 3/4 in.","costCenters":[],"links":[{"id":139765,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":282962,"type":{"id":4,"text":"Application Site"},"url":"https://pubs.usgs.gov/ds/041/application.zip"}],"scale":"0","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122.25,35 ], [ -122.25,44.5 ], [ -110.75,44.5 ], [ -110.75,35 ], [ -122.25,35 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671cd6","contributors":{"authors":[{"text":"Raines, Gary L.","contributorId":48162,"corporation":false,"usgs":true,"family":"Raines","given":"Gary","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":150057,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sawatzky, Don L.","contributorId":99110,"corporation":false,"usgs":true,"family":"Sawatzky","given":"Don","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":150059,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Connors, Katherine A.","contributorId":53785,"corporation":false,"usgs":true,"family":"Connors","given":"Katherine","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":150058,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":33101,"text":"b00O - 1996 - Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation","interactions":[{"subject":{"id":33101,"text":"b00O - 1996 - Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation","indexId":"b00O","publicationYear":"1996","noYear":false,"chapter":"O","title":"Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation"},"predicate":"IS_PART_OF","object":{"id":33201,"text":"b2000 - 1993 - Evolution of sedimentary basins: Paradox Basin","indexId":"b2000","publicationYear":"1993","noYear":false,"title":"Evolution of sedimentary basins: Paradox Basin"},"id":1}],"isPartOf":{"id":33201,"text":"b2000 - 1993 - Evolution of sedimentary basins: Paradox Basin","indexId":"b2000","publicationYear":"1993","noYear":false,"title":"Evolution of sedimentary basins: Paradox Basin"},"lastModifiedDate":"2021-11-24T20:07:41.454988","indexId":"b00O","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2000","chapter":"O","title":"Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation","docAbstract":"<p>The Ismay-Desert Creek interval and Cane Creek cycle of the Alkali Gulch interval of the Middle Pennsylvanian Paradox Formation in the Paradox Basin of Utah and Colorado contain excellent organic-rich source rocks having total organic carbon contents ranging from 0.5 to 11.0 percent. The source rocks in both intervals contain types I, II, and III organic matter and are potential source rocks for both oil and gas. Organic matter in the Ismay-Desert Creek interval and Cane Creek cycle of the Alkali Gulch interval (hereinafter referred to in this report as the \"Cane Creek cycle\") probably is more terrestrial in origin in the eastern part of the basin and is interpreted to have contributed to some of the gas produced there. </p><p>Thermal maturity increases from southwest to northeast for both the Ismay-Desert Creek interval and Cane Creek cycle, following structural and burial trends throughout the basin. In the northernmost part of the basin, the combination of a relatively thick Tertiary sedimentary sequence and high basinal heat flow has produced very high thermal maturities. Although general thermal maturity trends are similar for both the Ismay-Desert Creek interval and Cane Creek cycle, actual maturity levels are higher for the Cane Creek due to the additional thickness (as much as several thousand feet) of Middle Pennsylvanian section. </p><p>Throughout most of the basin, the Ismay-Desert Creek interval is mature and in the petroleum-generation window (0.10 to 0.50 production index (PI)), and both oil and gas are produced; in the south-central to southwestern part of the basin, however, the interval is marginally mature (&lt;0.10 PI) for petroleum generation, and mainly oil is produced. In contrast, the more mature Cane Creek cycle contains no marginally immature areas—it is mature (&gt;0.10 PI) in the central part of the basin and is overmature (past the petroleum-generation window (&gt;0.50 PI)) throughout most of the eastern part of the basin. The Cane Creek cycle generally produces oil and associated gas throughout the western and central parts of the basin and thermogenic gas in the eastern part of the basin. </p><p>Burial and thermal-history models were constructed for six different areas of the Paradox Basin. In the Monument upwarp area, the least mature part of the basin, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.10 and 0.20 PI and were buried to 13,400 ft and 14,300 ft, respectively. A constant heat flow through time of 40 mWm<sup>-2</sup> (milliwatts per square meter) is postulated for this area. Significant petroleum generation began at 45 Ma for the Ismay-Desert Creek interval and at 69 Ma for the Cane Creek cycle. </p><p>In the area around the confluence of the Green and Colorado Rivers, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.20 and 0.25 PI and were buried to 13,000 ft and 14,200 ft, respectively. A constant heat flow through time of 42 mWm<sup>-2</sup> is postulated for this area. Significant petroleum generation began at 60 Ma for the Ismay-Desert Creek interval and at 75 Ma for the Cane Creek cycle. </p><p>In the area around the town of Green River, Utah, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.60 and greater and were buried to 14,000 ft and 15,400 ft, respectively. A constant heat flow through time of 53 mWm<sup>-2</sup> is proposed for this area. Significant petroleum generation began at 82 Ma for the Ismay-Desert Creek interval and at 85 Ma for the Cane Creek cycle. </p><p>Around Moab, Utah, in the deeper, eastern part of the basin, the Ismay-Desert Creek interval and Cane Creek cycle have thermal maturities of 0.30 and around 0.35 PI and were buried to 18,250 ft and 22,000 ft, respectively. A constant heat flow through time of 40 mWm<sup>-2</sup> is postulated for this area. Significant petroleum generation began at 79 Ma for the Ismay-Desert Creek interval and at 90 Ma for the Cane Creek cycle. </p><p>At Lisbon Valley, also in the structurally deeper part of the basin, the Ismayy–Desert Creek interval and Cane Creek cycle have thermal maturities of 0.30 and greater than 0.60 PI and were buried to 15,750 ft and 21,500 ft, respectively. A constant heat flow through time of 44 mWm<sup>–2 </sup>is postulated for this area. Significant petroleum generation began at 79 Ma for the Ismay–Desert Creek interval and at 100 Ma for the Cane Creek cycle.</p><p>The area around Hermosa, Colo., in the southeastern part of the basin, has experienced a shallower burial history than the other areas in the basin, yet it has one of the highest thermal maturities. Here, the Ismay–Desert Creek interval and Cane Creek cycle have vitrinite reflectance values of 1.58 and 1.63 percent and were&nbsp; buried to 13,700 ft and 15,500 ft, respectively. Due to Tertiary igneous activity in this part of the basin, a variable heat flow is proposed: from 600 to 30 Ma, 45 mWm<sup>–2</sup>; from 30 to 25 Ma, 63 mWm<sup>–2</sup>; and from 25 Ma to present, 50 mWm<sup>–2</sup>. Significant petroleum generation began at 72 Ma for the Ismay–Desert Creek interval and at 76 Ma for the Cane Creek cycle.</p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Evolution of sedimentary basins: Paradox basin","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b00O","usgsCitation":"Nuccio, V.F., and Condon, S.M., 1996, Burial and thermal history of the Paradox Basin, Utah and Colorado, and petroleum potential of the Middle Pennsylvanian Paradox Formation: U.S. Geological Survey Bulletin 2000, iii, 41 p., https://doi.org/10.3133/b00O.","productDescription":"iii, 41 p.","costCenters":[],"links":[{"id":392102,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_22256.htm"},{"id":3297,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/bul/b2000o/b2000o.html","linkFileType":{"id":5,"text":"html"}},{"id":160624,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Colorado, Utah","otherGeospatial":"Paradox Basin","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -110.5,\n              36.417\n            ],\n            [\n              -107.5,\n              36.417\n            ],\n            [\n              -107.5,\n              39.250\n            ],\n            [\n              -110.5,\n              39.250\n            ],\n            [\n              -110.5,\n              36.417\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48b4e4b07f02db532964","contributors":{"authors":[{"text":"Nuccio, Vito F. vnuccio@usgs.gov","contributorId":853,"corporation":false,"usgs":true,"family":"Nuccio","given":"Vito","email":"vnuccio@usgs.gov","middleInitial":"F.","affiliations":[],"preferred":true,"id":209893,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Condon, Steven M.","contributorId":95464,"corporation":false,"usgs":true,"family":"Condon","given":"Steven","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":209894,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":22048,"text":"ofr96543 - 1996 - Preliminary paleontologic report on core T-24, Little Madeira Bay, Florida","interactions":[],"lastModifiedDate":"2020-03-27T06:58:52","indexId":"ofr96543","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-543","title":"Preliminary paleontologic report on core T-24, Little Madeira Bay, Florida","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96543","issn":"0094-9140","usgsCitation":"Ishman, S., Brewster-Wingard, G., Willard, D., Cronin, T.M., Edwards, L.E., and Holmes, C.W., 1996, Preliminary paleontologic report on core T-24, Little Madeira Bay, Florida: U.S. Geological Survey Open-File Report 96-543, 46 p. , https://doi.org/10.3133/ofr96543.","productDescription":"46 p. ","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"links":[{"id":153338,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":1212,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pdf/of/ofr96543.html","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Florida","otherGeospatial":"Little Madeira Bay","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -80.68702697753906,\n              25.158958480083598\n            ],\n            [\n              -80.58265686035156,\n              25.158958480083598\n            ],\n            [\n              -80.58265686035156,\n              25.205562422199467\n            ],\n            [\n              -80.68702697753906,\n              25.205562422199467\n            ],\n            [\n              -80.68702697753906,\n              25.158958480083598\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66cd7f","contributors":{"authors":[{"text":"Ishman, S. E.","contributorId":20346,"corporation":false,"usgs":true,"family":"Ishman","given":"S. E.","affiliations":[],"preferred":false,"id":186848,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brewster-Wingard, G. L.","contributorId":102508,"corporation":false,"usgs":true,"family":"Brewster-Wingard","given":"G. L.","affiliations":[],"preferred":false,"id":186852,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Willard, Debra  A. 0000-0003-4878-0942","orcid":"https://orcid.org/0000-0003-4878-0942","contributorId":85982,"corporation":false,"usgs":true,"family":"Willard","given":"Debra  A.","affiliations":[],"preferred":false,"id":186851,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Cronin, Thomas M. 0000-0002-2643-0979 tcronin@usgs.gov","orcid":"https://orcid.org/0000-0002-2643-0979","contributorId":2579,"corporation":false,"usgs":true,"family":"Cronin","given":"Thomas","email":"tcronin@usgs.gov","middleInitial":"M.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":186850,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Edwards, Lucy E. 0000-0003-4075-3317 leedward@usgs.gov","orcid":"https://orcid.org/0000-0003-4075-3317","contributorId":2647,"corporation":false,"usgs":true,"family":"Edwards","given":"Lucy","email":"leedward@usgs.gov","middleInitial":"E.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":186847,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Holmes, C. W.","contributorId":36076,"corporation":false,"usgs":true,"family":"Holmes","given":"C.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":186849,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"id":30357,"text":"wri964200 - 1996 - Hydrogeology and analysis of ground-water-flow system, Sagamore Marsh area, southeastern Massachusetts","interactions":[],"lastModifiedDate":"2018-05-17T14:08:59","indexId":"wri964200","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-4200","title":"Hydrogeology and analysis of ground-water-flow system, Sagamore Marsh area, southeastern Massachusetts","docAbstract":"<p>A study of the hydrogeology and an analysis of the ground-water-flow system near Sagamore Marsh, southeastern Massachusetts, was undertaken to improve the understanding of the current (1994­ 95) hydrogeologic conditions near the marsh and how the ground-water system might respond to proposed changes in the tidal-stage regime of streams that flood and drain the marsh. Sagamore Marsh is in a coastal area that is bounded to the east by Cape Cod Bay and to the south by the Cape Cod Canal. The regional geology is characterized by deltaic and glaciolacustrine sediments. The sediments consist of gravel, sand, silt, and clay and are part of the Plymouth-Carver regional aquifer system. The glacial sediments are hounded laterally by marine sand, silt, and clay along the coast. The principal aquifer in the area consists of fine to coarse glacial sand and is locally confined by fine-grained glaciolacustrine deposits consisting of silt and sandy clay and fine-grained salt-marsh sediments consisting of peat and clay. The aquifer is underlain by finer grained glaciolacustrine sediments in upland areas and by marine clay along the coast.</p><p>Shallow ground water discharges primarily along the edge of the marsh, whereas deeper ground water flows beneath the marsh and discharges to Cape Cod Bay. Tidal pulses originating from Cape Cod Bay and from tidal channels in the marsh are rapidly attenuated in the subsurface. Tidal ranges in Cape Cod Bay and in the tidal channels were on the order of 9 and 1.5 feet, respectively, whereas tidal ranges in the ground-water levels were less than 0.2 foot. Tidal pulses measured in the water table beneath a barrier beach between the marsh and Cape Cod Bay were more in phase with tidal pulses from Cape Cod Bay than with tidal pulses from the&nbsp;tidal channels in Sagamore Marsh, whereas tidal pulses in the regional aquifer were more in phase with tidal pulses from the tidal channels.&nbsp;</p><p>A 5-day aquifer test at a public-supply well adjacent to the marsh gave a transmissivity of the regional aquifer of 9,300 to 10,900 feet squared per day and a hydraulic conductivity of 181 to 213 feet per day, assuming a saturated thickness of the aquifer of 51.3 feet. The regional aquifer became unconfined near the pumped well during the test. The ratio of tidal ranges in the tidal channel to the ranges in the underlying aquifer at two sites (the lower and upper marsh) indicated aquifer diffusivities for the marsh sediments of 380 and 170 feet squared per day; these values correspond to hydraulic conductivities of 2.5 x 10<sup>-3</sup> and 1.7 x 10<sup>-3</sup> feet per day, respectively. The maximum distances from the tidal channel at the lower and upper marsh sites where tidal ranges would exceed 0.01 foot, as calculated from aquifer diffusivities and current (1995) tidal ranges in the tidal channels, were 24.4 and 26.7 feet, respectively. The maximum distances from the tidal channel where tidal pulses in the ground water would exceed 0.01 foot, using potential increased tidal stages resulting from proposed tidal-stage modifications and predicted by the U.S. Army Corps of Engineers, were 37.1 and 42.0 feet, respectively. </p><p>A numerical model of the marsh and surrounding aquifer system indicated that the contributing area for the supply well adjacent to the marsh, for current (1994) pumping conditions, extends toward Great Herring Pond, about 2 miles northwest (upgradient) of the well, and does not extend beneath the marsh. The model also indicates that the predicted increases in tidal stages in the marsh will have a negligible effect on local ground-water levels.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri964200","usgsCitation":"Walter, D.A., Masterson, J.P., and Barlow, P.M., 1996, Hydrogeology and analysis of ground-water-flow system, Sagamore Marsh area, southeastern Massachusetts: U.S. Geological Survey Water-Resources Investigations Report 96-4200, v, 41 p., https://doi.org/10.3133/wri964200.","productDescription":"v, 41 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"links":[{"id":345232,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1996/4200/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124666,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1996/4200/report-thumb.jpg"}],"country":"United States","state":"Massachusetts","otherGeospatial":"Sagamore Marsh","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db6275e0","contributors":{"authors":[{"text":"Walter, Donald A. 0000-0003-0879-4477 dawalter@usgs.gov","orcid":"https://orcid.org/0000-0003-0879-4477","contributorId":1101,"corporation":false,"usgs":true,"family":"Walter","given":"Donald","email":"dawalter@usgs.gov","middleInitial":"A.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":203111,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Masterson, John P. 0000-0003-3202-4413 jpmaster@usgs.gov","orcid":"https://orcid.org/0000-0003-3202-4413","contributorId":171510,"corporation":false,"usgs":true,"family":"Masterson","given":"John","email":"jpmaster@usgs.gov","middleInitial":"P.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true},{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":false,"id":203112,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Barlow, Paul M. 0000-0003-4247-6456 pbarlow@usgs.gov","orcid":"https://orcid.org/0000-0003-4247-6456","contributorId":1200,"corporation":false,"usgs":true,"family":"Barlow","given":"Paul","email":"pbarlow@usgs.gov","middleInitial":"M.","affiliations":[{"id":493,"text":"Office of Ground Water","active":true,"usgs":true}],"preferred":true,"id":203110,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":22162,"text":"ofr96513A - 1996 - Significant metalliferous and selected non-metalliferous lode deposits and placer districts for the Russian Far East, Alaska, and the Canadian Cordillera","interactions":[],"lastModifiedDate":"2022-11-23T19:41:55.079942","indexId":"ofr96513A","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-513","chapter":"A","title":"Significant metalliferous and selected non-metalliferous lode deposits and placer districts for the Russian Far East, Alaska, and the Canadian Cordillera","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96513A","usgsCitation":"Nokleberg, W.J., Bundtzen, T., Dawson, K.M., Eremin, R.A., Goryachev, N., Koch, R.D., Ratkin, V.V., Rozenblum, I.S., Shpikerman, V.I., Frolov, Y.F., Gorodinsky, M.E., Melnikov, V.D., Ognyanov, N.V., Petrachenko, E.D., Pozdeev, A.I., Ross, K.V., Wood, D.H., Grybeck, D., Khanchuk, A.I., Kovbas, L.I., Nekrasov, I.Y., and Sidorov, A.A., 1996, Significant metalliferous and selected non-metalliferous lode deposits and placer districts for the Russian Far East, Alaska, and the Canadian Cordillera: U.S. Geological Survey Open-File Report 96-513, 385 p., https://doi.org/10.3133/ofr96513A.","productDescription":"385 p.","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":409594,"rank":3,"type":{"id":36,"text":"NGMDB Index 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,{"id":24758,"text":"ofr96256 - 1996 - Mineral resource assessment of the Custer National Forest in the Pryor Mountains, Carbon County, south-central Montana","interactions":[],"lastModifiedDate":"2021-11-17T19:41:15.549644","indexId":"ofr96256","displayToPublicDate":"1997-03-01T00:00:00","publicationYear":"1996","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":"96-256","title":"Mineral resource assessment of the Custer National Forest in the Pryor Mountains, Carbon County, south-central Montana","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr96256","issn":"0094-9140","usgsCitation":"Van Gosen, B.S., Wilson, A., Hammarstrom, J.M., and Kulik, D.M., 1996, Mineral resource assessment of the Custer National Forest in the Pryor Mountains, Carbon County, south-central Montana: U.S. Geological Survey Open-File Report 96-256, iii, 76 p., https://doi.org/10.3133/ofr96256.","productDescription":"iii, 76 p.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":391811,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_22950.htm"},{"id":53784,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1996/0256/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":158266,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1996/0256/report-thumb.jpg"}],"country":"United States","state":"Montana","county":"Carbon County","otherGeospatial":"Custer National Forest, Pryor Mountains","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -108.638,\n              45.09\n            ],\n            [\n              -108.312,\n              45.09\n            ],\n            [\n              -108.312,\n              45.217\n            ],\n            [\n              -108.638,\n              45.217\n            ],\n            [\n              -108.638,\n              45.09\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66cf48","contributors":{"authors":[{"text":"Van Gosen, B. S. 0000-0003-4214-3811","orcid":"https://orcid.org/0000-0003-4214-3811","contributorId":97907,"corporation":false,"usgs":true,"family":"Van Gosen","given":"B.","middleInitial":"S.","affiliations":[],"preferred":false,"id":192509,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilson, A.B. 0000-0002-9737-2614","orcid":"https://orcid.org/0000-0002-9737-2614","contributorId":63818,"corporation":false,"usgs":true,"family":"Wilson","given":"A.B.","affiliations":[],"preferred":false,"id":192508,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hammarstrom, J. M.","contributorId":34513,"corporation":false,"usgs":true,"family":"Hammarstrom","given":"J.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":192506,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Kulik, D. M.","contributorId":46948,"corporation":false,"usgs":true,"family":"Kulik","given":"D.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":192507,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
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