Ground water suitable for public supply can be obtained from fractured metamorphic and igneous rooks at Mount Rushmore National Memorial, S. Dak.
\nThe memorial comprises three main drainage basins: Starling basin, Lafferty Gulch basin, and East Boundary basin. Ground water is most prevalent in Lafferty Gulch basin but Starling basin contributes the most surface water.
\nThe total water supply was obtained from springs until 1967 when increasing numbers of visitors required development of additional sources. As a result of this investigation, wells 3 and 4 were drilled in Lafferty Gulch basin and East Boundary basin. Well 3 is 200 feet deep in mica schist and granite. It produced 7.3 million gallons of water in 1968 and 7.7 million gallons of water in 1969, the total supply for the memorial. Well 4 is 500 feet deep, also in mica schist and granite. It is not used at the present time (1970) but will be used in the future when more water is needed. Water from both wells is potable, but the quality of water from well 3 is superior to that from well 4.
\nMica schist is the most abundant rock in the memorial. The more prominent hills and mountains, however, are in large, northerly striking granite sills, some of which are several hundred feet thick. Pegmatite sills and dikes are also numerous. The western boundary of the memorial is at the east edge of the Harney Peak Granite batholith. The dip of schistosity and bedding in schist adjacent to the batholith is about 30 ? E. but increases across the memorial to about 65 ? E. in the northeast corner.
\nAt some locations in the memorial, granite or pegmatite sills act as ground-water dams preventing the movement of ground water down gradient. A pegmatite or granite sill is probably the cause of the accumulation of water in the vicinity of well 3. The well flows when it is not being pumped.
\nThe occurrence of ground water is dependent upon the presence of joints and fractures in the schist and granite bedrock. The rocks themselves are relatively impermeable and would yield little or no water in their unaltered state.
\nMica schist that has been intruded by granite and (or) pegmatite is more fractured and yields more ground water in the memorial than mica schist alone. This condition may be due to jointing and to the greater fracturability of the intruded rocks in the vicinity of granitic intrusions.
\nGround water is also available from alluvium in major valleys such as Starling basin and the valleys of Grizzly Bear Creek and Battle Creek.
\nEvapotranspiration is the greatest use-item in the water budget. An approximation of evapotranspiration based upon an average annual precipitation of 19 inches is 1,600 acre-feet, or 80 percent of the annual precipitation.
\nSeveral locations in the memorial have potential as future, sources of ground-water supplies. The most promising areas are near spring 6 in the southeast corner and alluvium in the valleys of Battle and Grizzly Bear Creeks.
\nDeveloped and potential water resources in the memorial probably are sufficient to meet demands beyond the year 2000.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1865","usgsCitation":"Powell, J., Norton, J.J., and Adolphson, D.G., 1973, Water resources and geology of Mount Rushmore National Memorial, South Dakota: U.S. Geological Survey Water Supply Paper 1865, Report: vi, 49 p.; Plate: 34.00 x 22.00 inches, https://doi.org/10.3133/wsp1865.","productDescription":"Report: vi, 49 p.; Plate: 34.00 x 22.00 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":28723,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1865/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138810,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1865/report-thumb.jpg"},{"id":28724,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1865/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","otherGeospatial":"Mount Rushmore National Memorial","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.46400260925293,\n 43.873705074113886\n ],\n [\n -103.46400260925293,\n 43.88391319597796\n ],\n [\n -103.45061302185059,\n 43.88391319597796\n ],\n [\n -103.45061302185059,\n 43.873705074113886\n ],\n [\n -103.46400260925293,\n 43.873705074113886\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db687e04","contributors":{"authors":[{"text":"Powell, J.E.","contributorId":27030,"corporation":false,"usgs":true,"family":"Powell","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":145336,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Norton, James Jennings","contributorId":59412,"corporation":false,"usgs":true,"family":"Norton","given":"James","email":"","middleInitial":"Jennings","affiliations":[],"preferred":false,"id":145337,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Adolphson, D. G.","contributorId":106081,"corporation":false,"usgs":true,"family":"Adolphson","given":"D.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":145338,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":15242,"text":"ofr73205 - 1973 - Reconnaissance geology of the Balakot and Mahandri quadrangles, Hazara District, Pakistan","interactions":[{"subject":{"id":15242,"text":"ofr73205 - 1973 - Reconnaissance geology of the Balakot and Mahandri quadrangles, Hazara District, Pakistan","indexId":"ofr73205","publicationYear":"1973","noYear":false,"title":"Reconnaissance geology of the Balakot and Mahandri quadrangles, Hazara District, Pakistan"},"predicate":"SUPERSEDED_BY","object":{"id":5811,"text":"pp716C - 1975 - Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas","indexId":"pp716C","publicationYear":"1975","noYear":false,"chapter":"C","title":"Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas"},"id":1}],"supersededBy":{"id":5811,"text":"pp716C - 1975 - Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas","indexId":"pp716C","publicationYear":"1975","noYear":false,"title":"Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas"},"lastModifiedDate":"2012-02-02T00:06:52","indexId":"ofr73205","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-205","title":"Reconnaissance geology of the Balakot and Mahandri quadrangles, Hazara District, Pakistan","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr73205","usgsCitation":"Offield, T.W., and Abdullah, S., 1973, Reconnaissance geology of the Balakot and Mahandri quadrangles, Hazara District, Pakistan: U.S. Geological Survey Open-File Report 73-205, ii, 41 p. :maps (some folded) ;27 cm., https://doi.org/10.3133/ofr73205.","productDescription":"ii, 41 p. :maps (some folded) ;27 cm.","costCenters":[],"links":[{"id":147125,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6fe4b07f02db640a82","contributors":{"authors":[{"text":"Offield, Terry W.","contributorId":15196,"corporation":false,"usgs":true,"family":"Offield","given":"Terry","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":170803,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Abdullah, S.K.M.","contributorId":67896,"corporation":false,"usgs":true,"family":"Abdullah","given":"S.K.M.","email":"","affiliations":[],"preferred":false,"id":170804,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":56445,"text":"wdrAR721 - 1973 - Water resources data for Arkansas, water year 1972","interactions":[],"lastModifiedDate":"2012-02-02T00:12:22","indexId":"wdrAR721","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"AR-72-1","title":"Water resources data for Arkansas, water year 1972","language":"ENGLISH","doi":"10.3133/wdrAR721","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1973, Water resources data for Arkansas, water year 1972: U.S. Geological Survey Water Data Report AR-72-1, 149 p., https://doi.org/10.3133/wdrAR721.","productDescription":"149 p.","costCenters":[],"links":[{"id":184128,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fee4b07f02db5f7558","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":532626,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23312,"text":"ofr73102 - 1973 - Predicted effects of proposed navigation improvements on residence time and dissolved oxygen of the salt wedge in the Duwamish River estuary, King County, Washington","interactions":[],"lastModifiedDate":"2012-02-02T00:08:01","indexId":"ofr73102","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-102","title":"Predicted effects of proposed navigation improvements on residence time and dissolved oxygen of the salt wedge in the Duwamish River estuary, King County, Washington","docAbstract":"A model of the circulation and quality of water in the Duwamish River estuary has been sufficiently developed to allow prediction of the effects of a proposed widening and deepening of waterways on residence time and dissolved oxygen in the estuary's salt wedge. For a low river-discharge period in August 1970, use of the model yielded an estimated residence time of wedge water to be 6.3 days in the present waterways estuary and 8.6 days in the wider and deeper proposed-waterways estuary--a 37-percent increase. June-September 1970 and for the estuary about 4 miles upstream from its mouth, the model estimates indicate that dissolved-oxygen values in the wedge of the proposed-waterways estuary would be as much as 1.4 milligrams per liter lower and would average 0.4 milligram per liter lower than (average difference significant at 95-percent confidence level) dissolved-oxygen values in the wedge of the present-waterways estuary. \r\n\r\nExtrapolation to low dissolved-oxygen values of a regression between the predicted dissolved oxygen for both the proposed and present-waterways estuaries suggests that 4 miles upstream of the estuary mouth oxygen would be completely depleted from the proposed-waterways estuary wedge whereas there still would be 0.2 milligram of oxygen per liter of water in the wedge of the present-waterways estuary.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/ofr73102","issn":"0094-9140","usgsCitation":"Haushild, W., and Stoner, J., 1973, Predicted effects of proposed navigation improvements on residence time and dissolved oxygen of the salt wedge in the Duwamish River estuary, King County, Washington: U.S. Geological Survey Open-File Report 73-102, 13 p. :ill., map ;27 cm., https://doi.org/10.3133/ofr73102.","productDescription":"13 p. :ill., map ;27 cm.","costCenters":[],"links":[{"id":155134,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0102/report-thumb.jpg"},{"id":52612,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0102/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acee4b07f02db67fde2","contributors":{"authors":[{"text":"Haushild, W.L.","contributorId":48953,"corporation":false,"usgs":true,"family":"Haushild","given":"W.L.","affiliations":[],"preferred":false,"id":189874,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stoner, J.D.","contributorId":58261,"corporation":false,"usgs":true,"family":"Stoner","given":"J.D.","email":"","affiliations":[],"preferred":false,"id":189875,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":24797,"text":"ofr73358 - 1973 - Artificial recharge in the Waterman Canyon-East Twin Creek area, San Bernardino County, California","interactions":[],"lastModifiedDate":"2012-02-02T00:08:17","indexId":"ofr73358","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-358","title":"Artificial recharge in the Waterman Canyon-East Twin Creek area, San Bernardino County, California","docAbstract":"This is a study of the feasibility of recharging, in the Waterman Canyon-East Twin Creek area, imported water from northern California by way of the State Water Project beginning in 1972. \r\n\r\nThe feasibility of recharging 30,000 acre-feet of water a year in the Waterman Canyon-East Twin Creek area will depend on the effectiveness of fault K as a barrier to ground-water movement near the land surface. The results of test drilling and an infiltration test indicate that the subsurface material at the spreading grounds is permeable enough to allow recharged water to percolate to the water table. The data indicate that fault K extends into the Waterman Canyon-East Twin Creek area and may impede the lateral movement of recharged water. Fault K has no known surface expression and therefore probably does not affect the highly permeable younger alluvium. If that is so, fault K will be less effective as a barrier to ground-water movement as the recharge mound rises. Monitoring of the observation wells near the spreading grounds as the planned recharge operation proceeds should provide data about the hydrologic effects of fault K near the land surface.","language":"ENGLISH","publisher":"U.S. Geological Survey, Water Resources Division,","doi":"10.3133/ofr73358","issn":"0094-9140","usgsCitation":"Warner, J.W., and Moreland, J.A., 1973, Artificial recharge in the Waterman Canyon-East Twin Creek area, San Bernardino County, California: U.S. Geological Survey Open-File Report 73-358, iv, 44 p. :ill., maps ;27 cm., https://doi.org/10.3133/ofr73358.","productDescription":"iv, 44 p. :ill., maps ;27 cm.","costCenters":[],"links":[{"id":157510,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0358/report-thumb.jpg"},{"id":53810,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0358/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":53811,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0358/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672c47","contributors":{"authors":[{"text":"Warner, J. W.","contributorId":42996,"corporation":false,"usgs":true,"family":"Warner","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":192582,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moreland, J. A.","contributorId":71994,"corporation":false,"usgs":true,"family":"Moreland","given":"J.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":192583,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":15243,"text":"ofr73204 - 1973 - Reconnaissance geology of the Mansehra quadrangle, Hazara district, Pakistan","interactions":[{"subject":{"id":15243,"text":"ofr73204 - 1973 - Reconnaissance geology of the Mansehra quadrangle, Hazara district, Pakistan","indexId":"ofr73204","publicationYear":"1973","noYear":false,"title":"Reconnaissance geology of the Mansehra quadrangle, Hazara district, Pakistan"},"predicate":"SUPERSEDED_BY","object":{"id":5811,"text":"pp716C - 1975 - Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas","indexId":"pp716C","publicationYear":"1975","noYear":false,"chapter":"C","title":"Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas"},"id":1}],"supersededBy":{"id":5811,"text":"pp716C - 1975 - Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas","indexId":"pp716C","publicationYear":"1975","noYear":false,"title":"Geology of the southern Himalaya in Hazara, Pakistan, and adjacent areas"},"lastModifiedDate":"2012-02-02T00:06:52","indexId":"ofr73204","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-204","title":"Reconnaissance geology of the Mansehra quadrangle, Hazara district, Pakistan","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr73204","usgsCitation":"Offield, T.W., Abdullah, S., and Zafar, M., 1973, Reconnaissance geology of the Mansehra quadrangle, Hazara district, Pakistan: U.S. Geological Survey Open-File Report 73-204, 31 leaves :folded col. maps ;27 cm.; 41 p., https://doi.org/10.3133/ofr73204.","productDescription":"31 leaves :folded col. maps ;27 cm.; 41 p.","costCenters":[],"links":[{"id":147126,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6de4b07f02db63ed20","contributors":{"authors":[{"text":"Offield, Terry W.","contributorId":15196,"corporation":false,"usgs":true,"family":"Offield","given":"Terry","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":170805,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Abdullah, S.K.M.","contributorId":67896,"corporation":false,"usgs":true,"family":"Abdullah","given":"S.K.M.","email":"","affiliations":[],"preferred":false,"id":170806,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Zafar, M.S.","contributorId":93067,"corporation":false,"usgs":true,"family":"Zafar","given":"M.S.","email":"","affiliations":[],"preferred":false,"id":170807,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":15247,"text":"ofr73207 - 1973 - Geologic map of the Cotuit quadrangle, Barnstable County, Massachusetts","interactions":[{"subject":{"id":15247,"text":"ofr73207 - 1973 - Geologic map of the Cotuit quadrangle, Barnstable County, Massachusetts","indexId":"ofr73207","publicationYear":"1973","noYear":false,"title":"Geologic map of the Cotuit quadrangle, Barnstable County, Massachusetts"},"predicate":"SUPERSEDED_BY","object":{"id":62358,"text":"gq1213 - 1975 - Geologic map of the Cotuit quadrangle, Barnstable County, Cape Cod, Massachusetts","indexId":"gq1213","publicationYear":"1975","noYear":false,"title":"Geologic map of the Cotuit quadrangle, Barnstable County, Cape Cod, Massachusetts"},"id":1}],"supersededBy":{"id":62358,"text":"gq1213 - 1975 - Geologic map of the Cotuit quadrangle, Barnstable County, Cape Cod, Massachusetts","indexId":"gq1213","publicationYear":"1975","noYear":false,"title":"Geologic map of the Cotuit quadrangle, Barnstable County, Cape Cod, Massachusetts"},"lastModifiedDate":"2012-02-02T00:06:52","indexId":"ofr73207","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-207","title":"Geologic map of the Cotuit quadrangle, Barnstable County, Massachusetts","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr73207","usgsCitation":"Oldale, R.N., 1973, Geologic map of the Cotuit quadrangle, Barnstable County, Massachusetts: U.S. Geological Survey Open-File Report 73-207, 9 p. :ill., (1 folded), folded map ;28 cm.; 1 sheet, scale 1:24,000, https://doi.org/10.3133/ofr73207.","productDescription":"9 p. :ill., (1 folded), folded map ;28 cm.; 1 sheet, scale 1:24,000","costCenters":[],"links":[{"id":147154,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"scale":"24000","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b09e4b07f02db69c1a6","contributors":{"authors":[{"text":"Oldale, Robert N.","contributorId":38953,"corporation":false,"usgs":true,"family":"Oldale","given":"Robert","email":"","middleInitial":"N.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":170814,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2405,"text":"wsp2017 - 1973 - Improvement of trout streams in Wisconsin by augmenting low flows with ground water","interactions":[],"lastModifiedDate":"2015-10-01T13:24:03","indexId":"wsp2017","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2017","title":"Improvement of trout streams in Wisconsin by augmenting low flows with ground water","docAbstract":"Approximately 2 cubic feet per second of ground water were introduced into the Little Plover River in 1968 when natural streamflow ranged from 3 to 4 cubic feet per second. These augmentation flows were retained undiminished through the 2-mile reach of stream monitored. Maximum stream temperatures were reduced as much as 5?F (3?C) at the augmentation site during the test period, although changes became insignificant more than 1 mile downstream. Maximum temperatures might be reduced as much as 10?F (6?C) during critical periods, based on estimates using a stream temperature model developed as part of the study. During critical periods significant temperature improvement may extend 2 miles or more downstream. Changes in minimum DO (dissolved oxygen) levels were slight, primarily because of the high natural DO levels occurring during the test period. Criteria for considering other streams for flow augmentation are developed on the basis of the observed hydrologic responses in the Little Plover River. Augmentation flows of nearly 2? cubic feet per second of ground water were introduced into the headwater reach of Black Earth Creek from the end of June through mid-October 1969. Streamflow ranged from 1 to 2 cubic feet per second at the augmentation site, and the average flow at the gaging station at Black Earth, approximately 8 miles downstream, ranged from 25 to 50 cubic feet per second. Augmentation flows were retained through the 8-mile reach of stream. Temperature of the augmentation flow as it entered the stream ranged from 60? to 70?F (about 16? to 21?C) during the test period, and minimum stream temperatures were raised 5?F (3?C) or more at the augmentation site, with changes extending from 2 to 3 miles downstream. Augmentation during critical periods could maintain stream temperatures between 40? and 70?F (4? and 21?C) through most of the study reach. DO levels were increased by as much as 2 milligrams per liter or more below the augmentation site, although the improvement diminished to approximately 1 milligram per liter downstream in the problem reach. During critical periods DO improvement in the problem reach would be somewhat greater. Flow augmentation would not be necessary during normal conditions in either of the streams studied. Critical DO and temperature levels are not known to occur in the Little Plover River. Since the construction of secondary treatment facilities at the Cross Plains sewage-treatment plant, critical DO levels are no longer expected to be a problem in Black Earth Creek. However, results from this study may be used to estimate the effectiveness of flow augmentation in other streams in similar areas in which critical DO or temperature levels may occur.
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1973 - Base of fresh ground water approximately 3,000 micromhos in the Sacramento Valley and Sacramento-San Joaquin Delta, California","interactions":[],"lastModifiedDate":"2018-12-06T14:23:22","indexId":"wri7340","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-40","title":"Base of fresh ground water approximately 3,000 micromhos in the Sacramento Valley and Sacramento-San Joaquin Delta, California","docAbstract":"The study area consists of about 6,600 square miles; about 5,500 square miles of the floor of the Sacramento Valley, and about 1,100 square miles of the Sacramento-San Joaquin Delta. The Sacramento Valley, as defined by Bryan (1923, p. 8), extends from Red Bluff 145 miles southward to Suisun Bay. It is bounded on the east by the Sierra Nevada, on the northeast by the Cascade Range, on the northwest by the Klamath Mountains, and the west by the Coast Ranges. Southward the valley merges with the Delta and the San Joaquin Valley. The width of the Sacramento Valley varies from about 30 miles near Red Bluff to about 60 miles on the south, and averages about 40 miles. The southern boundary of the study area coincides with the northern boundary used in an earlier study be Page (1971, 1973a).
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Dakota\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f7e4b07f02db5f2301","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":532722,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2861,"text":"wsp1974 - 1973 - Water resources of the New Jersey part of the Ramapo River basin","interactions":[{"subject":{"id":56068,"text":"ofr70352 - 1970 - Water resources of the New Jersey part of the Ramapo River basin","indexId":"ofr70352","publicationYear":"1970","noYear":false,"title":"Water resources of the New Jersey part of the Ramapo River basin"},"predicate":"SUPERSEDED_BY","object":{"id":2861,"text":"wsp1974 - 1973 - Water resources of the New Jersey part of the Ramapo River basin","indexId":"wsp1974","publicationYear":"1973","noYear":false,"title":"Water resources of the New Jersey part of the Ramapo River basin"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:35","indexId":"wsp1974","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1974","title":"Water resources of the New Jersey part of the Ramapo River basin","docAbstract":"The Ramapo River, a major stream in the Passaic River basin, drains an area of 161 square miles, 70 percent of which is in Orange and Rockland Counties, N.Y., and 30 percent is in Bergen and Passaic Counties, N.J. This report describes the hydrology of the New Jersey part of the basin and evaluates the feasibility of developing large ground-water supplies from the stratified drift in the Ramapo River valley by inducing recharge to the aquifer from the river. The ground water and surface water of the basin are considered as a single resource because the development of either ground water or surface water affects the availability of the other. \r\n\r\nPrecambrian gneiss, sparsely mantled with Pleistocene glacial drift, underlies the basin west of the Ramapo River in New Jersey. To the east, bedrock consists of the Watchung Basalt and of shale, sandstone, and conglomerate of the Brunswick Formation of Triassic age. Glacial drift occurs nearly everywhere in the eastern part of the basin, and deposits of stratified drift more than 100 feet thick occur in the Ramapo valley. Average annual runoff at Pompton Lakes accounts for 25 inches of the 45 inches of annual precipitation in the New Jersey part of the basin, and the remaining 20 inches is accounted for by evapotranspiration. Streamflow is highly variable--particularly in the area underlain by gneissic rocks-because of the low storage capacity of the rocks and the rough topography. \r\n\r\nMany of the small tributaries go dry during extended periods of no precipitation. Small domestic supplies of ground water can be obtained nearly everywhere, but the Brunswick Formation is the only consolidated-rock aquifer in the basin that can be depended upon to yield 100-200 gallons per minute to wells. Supplies of more than 1,000 gallons per minute are available from wells tapping the stratified drift in the Ramapo valley. The drift supplies 75 percent of the ground water pumped for public supply in the basin. Sustained ground-water yield in upland areas, based on stream base-flow recession, is estimated to be 200,000-300,000 gallons per day per square mile for the drift-covered Brunswick Formation and about 100,000-200,000 gallons per day per square mile for the gneiss and basalt. Potential sustained yield of the stratified drift in the valley depends on the availability of the streamflow and on the induced rate of infiltration. \r\n\r\nPumping from the stratified drift results in a reduction in streamflow, which may be undesirable, mainly because of prior downstream water rights. On the basis of the storage available in the stratified drift and an analysis of daily flow during the drought period of October 1964 to September 1967 at Pompton Lakes, 20-25 million gallons per day of Ramapo River water are available for development after existing downstream water requirements are supplied. However, some low-flow augmentation will be. necessary to insure downstream rights. Rates of infiltration computed from seepage losses observed near Mahwah indicate that at least 11 million gallons per day, on an average basis, can be infiltrated from the river by the pumping of wells tapping the stratified drift. The use of recharge pits and spreading areas would increase the rate of infiltration. Losses from the Ramapo River could be minimized by returning treated sewage effluent directly to the river or, preferably, by recharging the stratified-drift aquifer with the treated effluent. \r\n\r\nGround-water quality and surface-water quality at times of low-flow vary according to the type of rock from which the water is obtained. Water from the gneiss is low in dissolved solids--less than 127 mg/l (milligrams per liter)--and soft to moderately hard--less than 94 rag/l. Water from the Brunswick Formation is more mineralized--total dissolved-solids content is as much as 278 mg/1 and hardness as much as 188 mg/1. Water from the stratified drift is generally intermediate in quality--that is, total dissolved-solids content is as ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1974","usgsCitation":"Vecchioli, J., and Miller, E., 1973, Water resources of the New Jersey part of the Ramapo River basin: U.S. Geological Survey Water Supply Paper 1974, vi, 77 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1974.","productDescription":"vi, 77 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":138982,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1974/report-thumb.jpg"},{"id":29456,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1974/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29457,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1974/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29458,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1974/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29459,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1974/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29460,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1974/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f2e4b07f02db5ef13d","contributors":{"authors":[{"text":"Vecchioli, John","contributorId":36113,"corporation":false,"usgs":true,"family":"Vecchioli","given":"John","email":"","affiliations":[],"preferred":false,"id":145920,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, E.G.","contributorId":44132,"corporation":false,"usgs":true,"family":"Miller","given":"E.G.","email":"","affiliations":[],"preferred":false,"id":145921,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2193,"text":"wsp2009C - 1973 - Chemical quality of surface water in the Flaming Gorge Reservoir area, Wyoming and Utah","interactions":[],"lastModifiedDate":"2017-09-04T11:04:36","indexId":"wsp2009C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2009","chapter":"C","title":"Chemical quality of surface water in the Flaming Gorge Reservoir area, Wyoming and Utah","docAbstract":"Construction of Flaming Gorge Dam on the Green River by the U.S. Bureau of Reclamation started in 1959, and storage began in November 1962. A reconnaissance study was made during the period 1966-68 to determine the effects of the reservoir on the chemical quality of the effluent water and to describe the quality of the impounded water and inflowing water.
The major inflow to the reservoir is from the Green River, which contributes an average of 81 percent of the water and 59 percent of the inflow load of dissolved solids. Together, Blacks Fork and Henrys Fork contribute an average of about 16 percent of the water and about 23 percent of the dissolved-solids load, whereas minor tributaries contribute approximately 3 percent of the total inflow water to the reservoir, but about 18 percent of the total incoming load of dissolved solids.
The concentration of dissolved solids in the reservoir in October 1966 was about 150 mg/l (milligrams per liter) greater than the concentration of the 1962-66 inflow and in September 1968 about 95 mg/l greater than the concentration of the 1962-68 inflow. The increased concentration is due. mostly to leaching of minerals from the reservoir bottom. For the 1963-68 water years, about 1.2 million tons of dissolved solids was leached from inundated areas. The major observable difference between the chemical composition of the inflow during 1963-66 and that of the reservoir in 1966 is an increase in the percentage of sulfate and a decrease in the percentage of bicarbonate. Impoundment of water in Flaming Gorge Reservoir during the 1963-68 water years caused the concentration of dissolved solids in the river system to increase by 130 mg/l, or about 32 percent over what would have occurred without the reservoir. Evaporation accounted for an increase of 15 mg/l, and leaching accounted for an increase of 115 mg/l.
","language":"English","publisher":"U.S. Goverment Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp2009C","usgsCitation":"Madison, R.J., and Waddell, K.M., 1973, Chemical quality of surface water in the Flaming Gorge Reservoir area, Wyoming and Utah: U.S. Geological Survey Water Supply Paper 2009, Report: iv, 18 p.; Plate: 22.00 in. x 20.00 in., https://doi.org/10.3133/wsp2009C.","productDescription":"Report: iv, 18 p.; Plate: 22.00 in. x 20.00 in.","numberOfPages":"24","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":138276,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2009c/report-thumb.jpg"},{"id":27834,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2009c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27835,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2009c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah, Wyoming","otherGeospatial":"Flaming Gorge Reservoir","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e47b3e4b07f02db49ee49","contributors":{"authors":[{"text":"Madison, R. J.","contributorId":84734,"corporation":false,"usgs":true,"family":"Madison","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":144803,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Waddell, Kidd M.","contributorId":20720,"corporation":false,"usgs":true,"family":"Waddell","given":"Kidd","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":144802,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2858,"text":"wsp1969 - 1973 - Water-supply development and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T11:55:59","indexId":"wsp1969","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1969","title":"Water-supply development and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan","docAbstract":"The Tri-County region, consisting of Clinton, Eaton, and Ingham Counties, is an area of 1,697 square miles in Michigan's Lower Peninsula and has as its hub the Lansing metropolitan area. The land surface ranges in altitude from about 700 to about 1,000 feet. The region receives an average of about 31 inches of precipitation each year.
The population is nearing 400,000 and by 1990 will be near 600,000. Average daily water use is slightly more than 30 million gallons today; by 1980 it will be about 50 million gallons, and by 1990 it will probably be about 70 million gallons.
The Tri-County region is drained by seven river systems. The median annual 7 -day mean low flows of the principal streams in these systems were measured at the point farthest downstream within the region. These values, in cubic feet per second, are as follows: Grand River, 180; Maple River, 34; Looking Glass River, 28; Red Cedar River, 30; Portage Creek, 15; Battle Creek, 20; and Thornapple River, 24-a total of 331 cubic feet per second or about 220 million gallons per day. The areal variance in 7-day low-flow runoff ranges from 0 to 0.15 cubic foot per second per square mile.
The principal source of ground water in the Tri-County region is a complex aquifer system composed of the Saginaw and Grand River Formations and some of the overlying glacial sediments. This aquifer yields between 300 and 700 gallons per minute to individual wells in much of the western half of Ingham County, in the eastern half of Clinton County, in a small area in southeastern Clinton County, and in northeastern Eaton County. In some parts of the region, the glacial sediments are favorable for development of moderate to large supplies of water. Minor aquifers in the region are the Bayport, Michigan, and Marshall Formations.
Providing water supplies in the future requires complete and comprehensive water-management programs. Such management programs involve determining which of several alternative water-development systems is the best. Some of the chief factors and methods that must be considered when planning these systems are combined use of ground and surface water, artificial recharge, treatment of wastes, use of storage reservoirs, and importation of water from the Great Lakes.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1969","usgsCitation":"Vanlier, K.E., Wood, W., and Brunett, J.O., 1973, Water-supply development and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan: U.S. Geological Survey Water Supply Paper 1969, Document: vii, 111 p.; 3 Plates: 35.70 x 31.97 inches or smaller, https://doi.org/10.3133/wsp1969.","productDescription":"Document: vii, 111 p.; 3 Plates: 35.70 x 31.97 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":139081,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1969/report-thumb.jpg"},{"id":247253,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1969/plate-1.pdf","size":"5337","linkFileType":{"id":1,"text":"pdf"}},{"id":247254,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1969/plate-2.pdf","size":"10148","linkFileType":{"id":1,"text":"pdf"}},{"id":247255,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1969/plate-3.pdf","size":"13282","linkFileType":{"id":1,"text":"pdf"}},{"id":29452,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1969/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","county":"Clinton County, Eaton County, Ingham County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-84.3681,43.1172],[-84.3675,42.9561],[-84.3679,42.9439],[-84.3666,42.861],[-84.3668,42.8561],[-84.3649,42.7746],[-84.1593,42.7779],[-84.1519,42.685],[-84.146,42.5999],[-84.1402,42.4239],[-84.2539,42.4236],[-84.2607,42.4242],[-84.3676,42.4242],[-84.3677,42.4224],[-84.4864,42.4215],[-84.6026,42.4215],[-84.7207,42.4209],[-84.83,42.421],[-84.8375,42.4215],[-84.9561,42.4221],[-85.0667,42.4215],[-85.0736,42.4211],[-85.0738,42.5956],[-85.0745,42.7707],[-84.9577,42.7712],[-84.8391,42.7706],[-84.8376,42.857],[-84.8393,42.9434],[-84.8382,43.1199],[-84.6022,43.1185],[-84.3681,43.1172]]]},\"properties\":{\"name\":\"Clinton\",\"state\":\"MI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f99fe","contributors":{"authors":[{"text":"Vanlier, Kenneth Eugene","contributorId":6840,"corporation":false,"usgs":true,"family":"Vanlier","given":"Kenneth","email":"","middleInitial":"Eugene","affiliations":[],"preferred":false,"id":145915,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wood, Warren W.","contributorId":47770,"corporation":false,"usgs":false,"family":"Wood","given":"Warren W.","affiliations":[{"id":6601,"text":"Michigan State University","active":true,"usgs":false}],"preferred":false,"id":145916,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brunett, Jilann O.","contributorId":92230,"corporation":false,"usgs":true,"family":"Brunett","given":"Jilann","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":145917,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2005,"text":"wsp2024 - 1973 - Water resources of the Big Sioux River Valley near Sioux Falls, South Dakota","interactions":[],"lastModifiedDate":"2017-10-15T12:37:57","indexId":"wsp2024","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2024","title":"Water resources of the Big Sioux River Valley near Sioux Falls, South Dakota","docAbstract":"The major sources of water in the Big Sioux River valley between Sioux Falls and Dell Rapids, S.Dak., are the Big Sioux River and the glacial outwash aquifer beneath the flood plain. The river and the aquifer are hydraulically connected.
\nThe Big Sioux River has an average annual discharge of 246 cubic feet per second, on the average exceeds bankfull stage every 2.3 years, and has moderate basin storage.. Periods of low flow are common in the late summer, fall, and winter. A low flow of 0.1 cubic foot per second has been recorded.
\nThe outwash aquifer is composed of permeable sand, sand and gravel, and some boulders. The aquifer underlies an area of 33 square miles and commonly has a saturated thickness of less than 30 feet.
\nAquifer tests and measurements of streamflow indicate a rate of streambed infiltration of about 6 gallons per day per square foot. Analyses of streambed samples and interpretations of lithology from an electric log indicate that the streambed sediments in the diversion channel of the Big Sioux River consist largely of relatively impermeable silts and clays.
\nUnder normal climatic conditions, most of the water pumped by the city of Sioux Falls is water that entered the aquifer by streambed infiltration.
\nTo evaluate the importance of the aquifer in the hydrologic system, both an electrical analog model and a digital model were programmed for storage depletion alone. These models were used to determine the water-level declines in the aquifer that would result from 1 year of withdrawal at a rate of 9-10 million gallons per day. Both models indicated that the existing well field can yield water at that rate for more than 1 year.
\nThe analog model was also used to determine the maximum average daily yield of the aquifer-river system for a 2-year period modeled for the minimum recorded stream discharge and for streambed infiltration as the only recharge. The maximum average yield under these conditions would be less than 24 million gallons per day. Most of the water pumped during this period would be from aquifer storage.
\nWater from the river is generally less mineralized, softer, and easier to treat than ground water. Water pumped from wells near the river is similar in quality to the river water, but does not have the objectionable odors or tastes often present in water from the river.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp2024","usgsCitation":"Jorgensen, D.G., and Ackroyd, E.A., 1973, Water resources of the Big Sioux River Valley near Sioux Falls, South Dakota: U.S. Geological Survey Water Supply Paper 2024, Report: vii, 50 p.; Plate: 44.26 x 25.00 inches, https://doi.org/10.3133/wsp2024.","productDescription":"Report: vii, 50 p.; Plate: 44.26 x 25.00 inches","numberOfPages":"59","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":27449,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2024/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27450,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2024/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138387,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2024/report-thumb.jpg"}],"country":"United States","state":"South Dakota","city":"Sioux Falls","otherGeospatial":"Big Sioux River Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.94335937499999,\n 43.50075243569041\n ],\n [\n -96.94335937499999,\n 43.97898113341921\n ],\n [\n -96.5643310546875,\n 43.97898113341921\n ],\n [\n -96.5643310546875,\n 43.50075243569041\n ],\n [\n -96.94335937499999,\n 43.50075243569041\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f4e4b07f02db5f0621","contributors":{"authors":[{"text":"Jorgensen, Donald G.","contributorId":19537,"corporation":false,"usgs":true,"family":"Jorgensen","given":"Donald","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":144513,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ackroyd, Earl A.","contributorId":59425,"corporation":false,"usgs":true,"family":"Ackroyd","given":"Earl","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":144514,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":56561,"text":"wdrNE722 - 1973 - Water resources data for Nebraska, water year 1972; part 2, water quality records","interactions":[],"lastModifiedDate":"2019-09-30T14:25:13","indexId":"wdrNE722","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"NE-72-2","title":"Water resources data for Nebraska, water year 1972; part 2, water quality records","docAbstract":"No abstract available.
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\nGlaciofluvial sediments underlying the bouldery till occur largely in the western half of the area. These sediments are generally less than 50 feet thick, and transmissivity is generally less than 50,000 gallons per day per foot.
\nSurficial glaciofluvial sediments are a source of ground water for high-yield wells only in the eastern part of the area in the vicinity of the Biwabik bedrock valley. Thickness of these sediments is greater than 100 feet in some places, but transmissivity is generally less than 50,000 gallons per day per foot.
\nPractical sustained yield of aquifers in glacial drift is estimated to be as much as 40 million gallons per day from known aquifers. Assuming that the ratio of area underlain by aquifer to total area is constant for the study area (about 20 percent where mapped in detail), as much as 80 million gallons per day could be developed from glacial-drift aquifers.
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