The water supply for the Pueblo Army Depot, 15 miles wast of Pueblo, Colo., is obtained from wells that tap an aquifer in terrace alluvium. Withdrawals have resulted in a water-level decline of 27 feet, which adversely affects the discharge rate of individual wells. Furthermore, excessive pumpage has resulted in progressive deterioration of water quality. Over a 20-year period, hardness has increased from 70 milligrams per liter to 135 milligrams per liter and dissolved-solids content has increased from 250 milligrams per liter to 370 milligrams per liter.
\nTwo new supply wells were drilled in the southern part of the Depot and were tested to determine aquifer properties and probable production rate. The hydraulic conductivity determined from these tests ranged from about 350 to nearly 600 gallons per day per square foot. The transmissivity for the full thickness of the aquifer is in the range of 7,500 to 12,000 gallons per day per foot.<.p>\n
\n
The two new supply wells can be pumped at a combined rate of about 140 gallons per minute. If pumpage in the existing well field is reduced by the same amount, some recovery of water levels in the field will occur and the trend in water quality deterioration may slow or even reverse.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/ofr72447","issn":"0094-9140","collaboration":"Prepared by the U.S. Geological Survey for the Department of the Army Pueblo Army Depot","usgsCitation":"Welder, F.A., and Hurr, R.T., 1972, Appraisal of shallow ground-water resources, Pueblo Army Depot, Colorado: U.S. Geological Survey Open-File Report 72-447, 44 p., https://doi.org/10.3133/ofr72447.","productDescription":"44 p.","numberOfPages":"53","costCenters":[],"links":[{"id":287752,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":287751,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0447/report.pdf"}],"country":"United States","state":"Colorado","otherGeospatial":"Pueblo Army Depot","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -104.75,38.0 ], [ -104.75,38.5 ], [ -104.25,38.5 ], [ -104.25,38.0 ], [ -104.75,38.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac6e4b07f02db67a38d","contributors":{"authors":[{"text":"Welder, Frank A.","contributorId":32173,"corporation":false,"usgs":true,"family":"Welder","given":"Frank","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":192617,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hurr, R. Theodore","contributorId":27023,"corporation":false,"usgs":true,"family":"Hurr","given":"R.","email":"","middleInitial":"Theodore","affiliations":[],"preferred":false,"id":192616,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":24047,"text":"ofr72269 - 1972 - Potential transport of sediment from Enloe Reservoir by the Similkameen and Okanogan rivers, Washington","interactions":[],"lastModifiedDate":"2015-03-13T17:31:03","indexId":"ofr72269","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"72-269","title":"Potential transport of sediment from Enloe Reservoir by the Similkameen and Okanogan rivers, Washington","docAbstract":"This study was undertaken to determine the probable effects on the Similkameen and Okanogan Rivers of the removal, transport, and deposition of sediment now deposited behind Enloe Dam on the Similkameen River, if the dam were removed.
\nUnder existing conditions of sediment transport, the average annual suspended-sediment discharges at three streamflow-measuring sites are calculated to be 134,000 tons for the Similkameen River near Nighthawk, 175,000 tons for the Okanogan River near Tonasket, and 175,000 tons for the Okanogan River at Malott.
\nThe volume of sediment in Enloe Reservoir was computed to be 1.79 million cubic yards (about 2.4 million tons). The sediment is largely sand. If the dam were removed the maximum amount of reservoir sand transportable (in addition to normal sediment discharge), under stated conditions of velocity and depth during any average 10-year period, would range from about 17,000 to 580,000 cubic yards per year, with about 320,000 cubic yards being transported during a year of average water discharge. These volumes represent a range of 32 to less than 1 percent of the volume of sediment now deposited in the reservoir.
\nThe reservoir deposits not carried to the mouth of the Okanogan River (at Columbia River) would be deposited largely in a 17-mile reach of the Okanogon River immediately downstream from its confluence with the Similkameen River. Deposition of the reservoir sediment would tend to reduce the capacity of the channel of the Okanogan River in this reach; also there possibly would be some long-tern adjustments of the stream course to the temporary increase in the sediment load. Locally, the reduction in the channel cross section probably would increase the depth of the water and area of inundation during floods. Deposition of sediment in the Okanogan River channel and accompanying undesirable effects would be less severe if the dam were removed in segments over a period of several years.
\nIf the dam is removed in segments the amount of sediment transported by the river could be monitored to evaluate (1) the timing of the removal of the remaining segments of the dam, based on actual sediment-transport data, (2) the amount of sediment rremaining in the reservoit, and (3) the impact of sediment deposition on channel configuration and flooding.
","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/ofr72269","issn":"0094-9140","usgsCitation":"Nelson, L.M., 1972, Potential transport of sediment from Enloe Reservoir by the Similkameen and Okanogan rivers, Washington: U.S. Geological Survey Open-File Report 72-269, iii, 17 p. :ill., maps ;27 cm.;, https://doi.org/10.3133/ofr72269.","productDescription":"iii, 17 p. :ill., maps ;27 cm.;","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"links":[{"id":156319,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":298548,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0269/ofr72-269.pdf","text":"Report","size":"670 KB","linkFileType":{"id":1,"text":"pdf"},"description":"PDF of Report"},{"id":298549,"rank":3,"type":{"id":14,"text":"Image"},"url":"https://pubs.usgs.gov/of/1972/0269/ofr72-269_fig2.pdf","text":"Figure 2","size":"90 KB","linkFileType":{"id":1,"text":"pdf"},"description":"PDF of Figure 2"}],"contact":"Director, Washington Water Science Center
U.S. Geological Survey
934 Broadway, Suite 300
Tacoma, Washington 98402
http://wa.water.usgs.gov/
Floods and high water occurred throughout the summer of 1971 in south-central Alaska. Snow cover, 150 percent of average, in the mountains on May 1 caused local snowmelt floods from mid-May to mid-July. The peak discharge of 265,000 cfs (cubic feet per second) on July 15 at Copper River near Chitina was the highest in 22 years of record.
However, the major flood period was August 8-11. Precipitation totals of 3 to 9 inches during August 5-11 were recorded in an area extending northeastward from Iliamna Lake to Palmer, Talkeetna, and Paxson Lake. The principal flood areas were the upper Copper, Matanuska, Susitna, Chakachatna, and Kvichak River basins. Flooding in the Anchorage area was not severe. Total damage caused by the August flood is estimated to be 8 to 10 million dollars of which 6 million dollars occurred in the Matanuska Valley.
Extreme floods occurred in the Matanuska Valley. A lake near Sutton on an unnamed tributary to Granite Creek breached its embankment, which released a peak discharge in Granite Creek on August 10 of 58,600 cfs, 23.4 times the probable 50-year flood. Other streams near Sutton, tributary to the Matanuska River, had peak discharges 1.8 to 8.9 times the probable 50-year flood. The Matanuska River at Palmer had a peak discharge of 82,100 cfs, 1.2 times the probable 50-year flood. Downstream near Bodenburg Butte, an area was inundated when the Matanuska River overtopped a dike. Another extreme flood occurred at the Chakachatna River near Tyonek on August 11 where the peak discharge was estimated to be 470,000 cfs. The peak was caused by lateral erosion of a channel constriction formed by Barrier Glacier at the outlet of Chakachamna Lake.
Hydrologic data for planning, discussions of antecedent conditions, and meteorology along with a description of the floods and flood damage are included. Tables of storm precipitation, peak discharge data, sediment data, and discharge for the June-August period are also included.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr72215","usgsCitation":"Lamke, R.D., 1972, Floods in the summer of 1971 in south-central Alaska: U.S. Geological Survey Open-File Report 72-215, 88 p., https://doi.org/10.3133/ofr72215.","productDescription":"88 p.","costCenters":[],"links":[{"id":156164,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0215/report-thumb.jpg"},{"id":423801,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0215/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Alaska","otherGeospatial":"south-central 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In Part 1, records are included for 71 gaging stations of which 67 are streamflow discharge stations, and 4 are reservoir or lake stations; also are included records for 27 low-flow partial-record stations, 143 crest-stage partial-record stations, and 91 miscellaneous sites. Locations of gaging stations are shown in Figure 1. In Part 2, data on the quality of surface water (chemical and temperature) were collected from designated sampling sites at pre-determined intervals such as monthly, or less frequently, and at one site data were recorded on punched paper tape at 60-minute intervals. Records are given for 55 sampling stations of which 5 are continuous record stations, 26 are partial-record stations, and 3 are miscellaneous sites. Locations of water-quality stations are shown in Figure 1. A few pertinent stations (not included above) in bordering States are also included in this report. The records were collected and computed by the Water Resources Division of the U.S. Geological Survey under the direction of L. E. Carroon, district chief. These data represent that portion of the National Water Data System collected by the U.S. Geological Survey and cooperating State and Federal agencies in Mississippi.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f9e4b07f02db5f3bb8","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":532871,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2715,"text":"wsp1827D - 1972 - Effect of aging on aluminum hydroxide complexes in dilute aqueous solutions","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"wsp1827D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1827","chapter":"D","title":"Effect of aging on aluminum hydroxide complexes in dilute aqueous solutions","docAbstract":"Aqueous aluminum solutions containing 4?10 -5 mole/liter aluminum and a constant total ionic strength of 10 -2, but with varying ratios of hydroxide to aluminum (OH:Al), were prepared. Progress of these solutions toward equilibrium conditions over aging periods of as much as 2 years was studied by determining the composition and pH of the solutions at various time intervals. The solutions, after mixing, were supersaturated with respect to both crystalline and amorphous forms of aluminum oxides and aluminum hydroxides. The compositions of the solutions were determined by use of a timed colorimetric analytical procedure which allowed the estimation of three separate forms of aluminum that have been designated Al a, Al b, and Al c. Form Al a appeared to be composed of monomeric species such as Al(H20)6+3, Al(OH)(H20)5+2, Al(OH)2(H20)4 +I and Al(OH)4-. Form Al b was polynuclear material containing perhaps 20-400 aluminum atoms per structure. It appeared to be a metastable material. Form Al c was composed of relatively large, microcrystalline, clearly solid AI(OH)3 particles.\r\n\r\nFor each OH :Al ratio, the concentration of Al a remained constant with aging time, Al b decreased, and Al c increased. It appeared that Al b particles were increasing in size and ultimately were converted to Al c particles. After a few weeks' aging, Al c particles had the structure of gibbsite. \r\n\r\nIn all solutions, equilibrium was only very slowly achieved, and the time required depended on the OH:Al ratio and how rapidly the solution was initially prepared (mixing time). Lower ratios caused a slower approach to equilibrium; sometimes equilibrium was not achieved even after several years' aging. The more slowly base was initially added (to obtain the proper OH:Al ratio), the more slowly was equilibrium approached. Ultimate equilibrium values of dissolved aluminum concentration and pH were consistent with known thermodynamic data on monomeric aluminum species. \r\n\r\nFrom data determined during the aging study and by considering Al b material to consist of extremely small solid gibbsite particles, it was possible to estimate the Gibbs free energy of the (001) crystal face (?F, the gibbsite 'face') and the. Gibbs free energy of the (110) and (100) crystal faces (?E, the gibbsite 'edge') of gibbsite in equilibrium with its saturated solution. These values were: ?F=1404 ? 24 ergs/cm 2, and ?E = 483 ?-84 ergs/cm 2.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1827D","usgsCitation":"Smith, R.W., and Hem, J.D., 1972, Effect of aging on aluminum hydroxide complexes in dilute aqueous solutions: U.S. Geological Survey Water Supply Paper 1827, iv, 51 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1827D.","productDescription":"iv, 51 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":139001,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1827d/report-thumb.jpg"},{"id":29099,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1827d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db688247","contributors":{"authors":[{"text":"Smith, Ross Wilbert","contributorId":61404,"corporation":false,"usgs":true,"family":"Smith","given":"Ross","email":"","middleInitial":"Wilbert","affiliations":[],"preferred":false,"id":145656,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hem, John David","contributorId":42577,"corporation":false,"usgs":true,"family":"Hem","given":"John","email":"","middleInitial":"David","affiliations":[],"preferred":false,"id":145655,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1470,"text":"wsp1980 - 1972 - Ground-water levels in the United States, 1966-70, northwestern states","interactions":[],"lastModifiedDate":"2024-01-26T19:36:42.831555","indexId":"wsp1980","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1980","title":"Ground-water levels in the United States, 1966-70, northwestern states","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1980","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1972, Ground-water levels in the United States, 1966-70, northwestern states: U.S. Geological Survey Water Supply Paper 1980, v, 228 p., https://doi.org/10.3133/wsp1980.","productDescription":"v, 228 p.","costCenters":[],"links":[{"id":425033,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25204.htm","text":"Idaho","linkFileType":{"id":5,"text":"html"}},{"id":425034,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25205.htm","text":"Montana","linkFileType":{"id":5,"text":"html"}},{"id":425038,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25209.htm","text":"Wyoming","linkFileType":{"id":5,"text":"html"}},{"id":425037,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25208.htm","text":"Washington","linkFileType":{"id":5,"text":"html"}},{"id":425036,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25207.htm","text":"Utah","linkFileType":{"id":5,"text":"html"}},{"id":425035,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25206.htm","text":"Oregon","linkFileType":{"id":5,"text":"html"}},{"id":425032,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25203.htm","text":"Colorado","linkFileType":{"id":5,"text":"html"}},{"id":425031,"rank":3,"type":{"id":36,"text":"NGMDB Index 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa8e4b07f02db66755c","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":527852,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1946,"text":"wsp1873E - 1972 - Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina","interactions":[{"subject":{"id":55881,"text":"ofr68327 - 1968 - Interim report on sea-water encroachment into the Cape Fear River Estuary, North Carolina","indexId":"ofr68327","publicationYear":"1968","noYear":false,"title":"Interim report on sea-water encroachment into the Cape Fear River Estuary, North Carolina"},"predicate":"SUPERSEDED_BY","object":{"id":1946,"text":"wsp1873E - 1972 - Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina","indexId":"wsp1873E","publicationYear":"1972","noYear":false,"chapter":"E","title":"Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina"},"id":1}],"lastModifiedDate":"2019-12-30T10:14:20","indexId":"wsp1873E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1873","chapter":"E","title":"Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina","docAbstract":"This report presents the results of a fluorescent-dye-tracing study to determine the concentrations of a pollutant that would be present in the Northeast Cape Fear Estuary at various rates of continuous waste injection and freshwater inflow. Rhodamine WT dye was introduced into the estuary at a constant rate over a 24.8-hour period (two tidal cycles) at a point 6.4 miles upstream from the mouth in Wilmington, N.C., and concentrations were monitored at several selected sections in the tide-affected part of the river for 17 days. The range between high and low tide in this reach of the estuary averages at-rut 3.5 feet, and there is usually strong flow in both directions. \r\n\r\nResults of the dye study indicate that if a pollutant were injected at a rate of 100 pounds per day under the conditions of relatively low inflow existing' at the time, concentrations would ultimately build up to 20 micrograms of dye per liter of water 1,000 feet downstream. The flushing time during the study is estimated to be 17 days. These results are extrapolated to include periods of lower or higher inflow. For example, at average intervals of 10 years, it is estimated that inflow is so low that 100 days are required for a pollutant to travel the 6.4 miles from the point of waste release to the mouth of the river. Under these conditions it is expected that 1,000 feet downstream from the point of waste discharge, daily maximum concentrations will average about 130 micrograms per liter for each 100 pounds of pollutant injected per day. \r\n\r\nResults of a continuous discharge measurement of flow made by current meter during a complete tidal cycle are presented as a part of this report. Data from this measurement and other evidence indicate that net upstream flow in the estuary is possible over a period of several days.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1873E","usgsCitation":"Hubbard, E., and Stamper, W.G., 1972, Movement and dispersion of soluble pollutants in the Northeast Cape Fear Estuary, North Carolina: U.S. Geological Survey Water Supply Paper 1873, v, 31 p. , https://doi.org/10.3133/wsp1873E.","productDescription":"v, 31 p. ","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":138417,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1873e/report-thumb.jpg"},{"id":27277,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1873e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Carolina","otherGeospatial":"Cape Fear Estuary","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -78.3599853515625,\n 33.77458136371689\n ],\n [\n -77.7227783203125,\n 33.77458136371689\n ],\n [\n -77.7227783203125,\n 34.5020297944346\n ],\n [\n -78.3599853515625,\n 34.5020297944346\n ],\n [\n -78.3599853515625,\n 33.77458136371689\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b47ea","contributors":{"authors":[{"text":"Hubbard, E. F.","contributorId":66666,"corporation":false,"usgs":true,"family":"Hubbard","given":"E. F.","affiliations":[],"preferred":false,"id":144416,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stamper, William G.","contributorId":58259,"corporation":false,"usgs":true,"family":"Stamper","given":"William","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":144415,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1995,"text":"wsp1798J - 1972 - Sediment transport in the western tributaries of the Sacramento River, California","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1798J","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1798","chapter":"J","title":"Sediment transport in the western tributaries of the Sacramento River, California","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1798J","usgsCitation":"Jones, B.L., Hawley, N., and Crippen, J.R., 1972, Sediment transport in the western tributaries of the Sacramento River, California: U.S. Geological Survey Water Supply Paper 1798, iv, J 1-J 27 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1798J.","productDescription":"iv, J 1-J 27 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":138484,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1798j/report-thumb.jpg"},{"id":27396,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1798j/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbe98","contributors":{"authors":[{"text":"Jones, Benjamin L.","contributorId":78313,"corporation":false,"usgs":true,"family":"Jones","given":"Benjamin","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":144493,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hawley, N.L.","contributorId":82286,"corporation":false,"usgs":true,"family":"Hawley","given":"N.L.","email":"","affiliations":[],"preferred":false,"id":144494,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Crippen, John R.","contributorId":13208,"corporation":false,"usgs":true,"family":"Crippen","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144492,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1678,"text":"wsp1970A - 1972 - Floods of May 1968 in south Arkansas","interactions":[],"lastModifiedDate":"2012-02-02T00:05:23","indexId":"wsp1970A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1970","chapter":"A","title":"Floods of May 1968 in south Arkansas","docAbstract":"The floods of May 1968 in south Arkansas produced the greatest peak discharges in the history of recorded streamflow at several gaging stations. Most notable of these floods was on Cossatot River near DeQueen, which has a continuous record since 1938. The peak discharge of 122,000 cubic feet per second was almost twice the previous maximum discharge of 62,000 cubic feet per second in 1961. At Lake Greeson near Murfreesboro, water flowed over the spillway for the first time since construction of the dam in 1949. The lake reached au elevation of 564.60 feet, which is 1.60 feet above the spillway crest. The previous maximum stage of 557.84 feet occurred in 1953. No lives were lost as a result of the flood, but property damage amounted to about .$18 million. \r\n\r\nHeavy rains began on May 7 and continued to May 18. The periods of heaviest rainfall were May 9-10, 13, and 16-17. The maximum 24-hour rainfall recorded was 10.1 inches at Gillham Dam near DeQueen on May 13.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1970A","usgsCitation":"Gilstrap, R., 1972, Floods of May 1968 in south Arkansas: U.S. Geological Survey Water Supply Paper 1970, vi, 94 p. :illus., maps (1 fold. in pocket) ;24 cm., https://doi.org/10.3133/wsp1970A.","productDescription":"vi, 94 p. :illus., maps (1 fold. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138263,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1970a/report-thumb.jpg"},{"id":26754,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1970a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26755,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1970a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d9e4b07f02db5df95a","contributors":{"authors":[{"text":"Gilstrap, R.C.","contributorId":23124,"corporation":false,"usgs":true,"family":"Gilstrap","given":"R.C.","email":"","affiliations":[],"preferred":false,"id":143962,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2075,"text":"wsp1939D - 1972 - Chemical quality of the water in the Tucson basin, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:05:23","indexId":"wsp1939D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1939","chapter":"D","title":"Chemical quality of the water in the Tucson basin, Arizona","docAbstract":"The Tucson basin is a broad mountain-rimmed area of about 1,000 square miles in the Basin and Range physiographic province in southeastern Arizona. The altitude ranges from 2,000 feet in the basin to as much as 8,000 feat in the mountains. The major streams in the area are the Santa Cruz River and its principal tributaries--Cafiada del Oro, Rillito Creek, and Pantano Wash. The climate is semiarid, and the distribution and amount of precipitation vary greatly. The potential evapotranspiration is about four times the average annual precipitation. \r\n\r\nThe streamflow is of excellent chemical quality, although most of the flow occurs during floods and generally has large concentrations of suspended sediment. Because of the erratic occurrence and quantity of streamflow and because of the lack of surface-water storage reservoirs, all the water for municipal, industrial, and agricultural uses is obtained from the many wells that tap the permeable sedimentary deposits, which constitute the principal aquifer in the Tucson basin. \r\n\r\nThe aquifer consists of three sedimentary formations that range in age from middle Tertiary to Quaternary. The aquifer is as much as 2,000 feet thick and is composed mainly of sand, gravel, sandstone, and conglomerate. The upper part of the aquifer is more permeable than the lower part, and most wells obtain water at depths of less than 700 feet below the land surface. \r\n\r\nMost ground water contains less than 500 mg/l (milligrams per liter) of dissolved solids and is of suitable chemical quality for most uses. The water to depths of as much as 700 feet is a calcium sodium bicarbonate type, is hard to moderately hard, and contains less than 1.0 mg/l fluoride. Water at greater depth is a sodium bicarbonate type, is soft, and is of excellent chemical quality; however, water below about 1,0.00 feet may contain fluoride in excess of the maximum allowable limit of 1.4 mg/l for public supply. \r\n\r\nThe ground water of poorest quality for public supply is at shallow depths along the major streams, in the Pantano Formation along the northeast margin of the basin, at depth in gypsiferous mudstone, and along a narrow zone that trends northwestward across the basin. Water from these hydrologic environ- may contain as much as 500 mg/1 dissolved solids an4 in places may contain more than 1,000 mg/1 dissolved solids. \r\n\r\nThe anomalously large concentrations of calcium, bicarbonate, nitrate and sulfate in the ground water along the major streams, where the water table is from 25 to 150 feet below the land surface, are the result of near-surface phenomena. The large concentrations of these ions are derived from solution of relict salts, which were deposited in marshes along the streams prior to about 1900 by infiltrating surface water. In the narrow zone the trends northwestward across the basin, the large concentrations of calcium and sulfate are the result of the solution of limestone and gypsiferous mudstone in the sedimentary rocks in the headwaters area of Pantano Wash. The largest nitrate concentrations occur in the ground water along the Santa Cruz River; the nitrate probably is derived from irrigation return water, decayed vegetation from the marshes that occupied parts of the channel prior to 1900, and sewage effluent. \r\n\r\nAnomalously large concentrations of sodium, sulfate, chloride, and fluoride occur in ground water along the Santa Cruz River near the major faults that displace the older formations. These anomalously large concentrations probably are derived from the upward leakage of deep water that has reacted with the gypsiferous mudstone in the center of the basin and moved along the faults into the near-surface deposits. \r\n\r\nIn the Tucson basin the water is divided into seven chemical types based on the relative amount of four major ions--calcium, sodium, bicarbonate, and sulfate---and the absolute amount of chloride. Most of the water is either a calcium sodium bicarbonate or a sodium bicarbonate type. \r\n\r\nGr","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1939D","usgsCitation":"Laney, R., 1972, Chemical quality of the water in the Tucson basin, Arizona: U.S. Geological Survey Water Supply Paper 1939, 1 portfolio (iv, 46 p. illus. 5 plates) ;23 cm., https://doi.org/10.3133/wsp1939D.","productDescription":"1 portfolio (iv, 46 p. illus. 5 plates) ;23 cm.","costCenters":[],"links":[{"id":110054,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25166.htm","linkFileType":{"id":5,"text":"html"},"description":"25166"},{"id":138343,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1939d/report-thumb.jpg"},{"id":27632,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27633,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939d/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27634,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939d/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27635,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1939d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247101,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939d/plate-5.pdf","size":"4732","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e32a2","contributors":{"authors":[{"text":"Laney, R. L.","contributorId":83889,"corporation":false,"usgs":true,"family":"Laney","given":"R. L.","affiliations":[],"preferred":false,"id":144643,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2597,"text":"wsp2019A - 1972 - Estimating steady-state evaporation rates from bare soils under conditions of high water table","interactions":[],"lastModifiedDate":"2012-02-02T00:05:20","indexId":"wsp2019A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"2019","chapter":"A","title":"Estimating steady-state evaporation rates from bare soils under conditions of high water table","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp2019A","usgsCitation":"Ripple, C., Rubin, J., and Van Hylckama, T.E., 1972, Estimating steady-state evaporation rates from bare soils under conditions of high water table: U.S. Geological Survey Water Supply Paper 2019, v, 39 p. :ill. ;24 cm., https://doi.org/10.3133/wsp2019A.","productDescription":"v, 39 p. :ill. ;24 cm.","costCenters":[],"links":[{"id":137595,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2019a/report-thumb.jpg"},{"id":28877,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2019a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc880","contributors":{"authors":[{"text":"Ripple, C.D.","contributorId":11586,"corporation":false,"usgs":true,"family":"Ripple","given":"C.D.","email":"","affiliations":[],"preferred":false,"id":145465,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rubin, Jacob","contributorId":23918,"corporation":false,"usgs":true,"family":"Rubin","given":"Jacob","email":"","affiliations":[],"preferred":false,"id":145466,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Van Hylckama, T. E. A.","contributorId":73568,"corporation":false,"usgs":true,"family":"Van Hylckama","given":"T.","email":"","middleInitial":"E. A.","affiliations":[],"preferred":false,"id":145467,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2110,"text":"wsp1982 - 1972 - Chemical quality of water in the Walnut River basin, south-central Kansas","interactions":[{"subject":{"id":55854,"text":"ofr68167 - 1968 - Chemical quality of water in the Walnut River basin, south-central Kansas","indexId":"ofr68167","publicationYear":"1968","noYear":false,"title":"Chemical quality of water in the Walnut River basin, south-central Kansas"},"predicate":"SUPERSEDED_BY","object":{"id":2110,"text":"wsp1982 - 1972 - Chemical quality of water in the Walnut River basin, south-central Kansas","indexId":"wsp1982","publicationYear":"1972","noYear":false,"title":"Chemical quality of water in the Walnut River basin, south-central Kansas"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:24","indexId":"wsp1982","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1982","title":"Chemical quality of water in the Walnut River basin, south-central Kansas","docAbstract":"Improper disposal of oil-field brine and other wastes has adversely affected \r\nthe naturally diverse chemical quality of much of the water in the Walnut \r\nRiver basin, south-central Kansas. \r\nThe basin is an area of about 2,000 square miles in the shape of a rough \r\ntriangle with its apex toward the south. The Whitewater River, a principal \r\ntributary, and the Walnut River below its junction with the Whitewater River \r\nflow southward toward the Arkansas River along courses nearly coincident with \r\nthe contact of the Chase and overlying Sumner Groups of Permian age. The \r\ncourses of many minor tributaries are parallel to a well-developed joint system \r\nin the Permian rock. \r\nThick interbedded limestone and shale of the Chase Group underlie the more \r\nextensive, eastern part of the basin. Natural waters are dominantly of the \r\ncalcium bicarbonate type. Shale and subordinate strata of limestone, gypsum, \r\nand dolomite of the Sumner Group underlie the western part of the basin. \r\nNatural waters are dominantly of the calcium sulfate type. Inflow from most \r\neast-bank tributaries dilutes streamflow of the Walnut River; west-bank tributaries, including the Whitewater River, contribute most of the sulfate. \r\nTerrace deposits and alluvial fill along the stream channels are assigned to \r\nthe Pleistocene and Holocene Series. Calcium bicarbonate waters are common \r\nas a result of the dissolution of nearly ubiquitous fragments of calcareous rock, \r\nbut the chemical quality of the water in the discontinuous aquifers depends \r\nmainly on the quality of local recharge. \r\nConcentrations of dissolved solids and of one or more ions in most well waters \r\nexceeded recommended maximums for drinking water. Nearly all the ground \r\nwater is hard to very hard. High concentrations of sulfate characterize waters \r\nfrom gypsiferous aquifers; high concentrations of chloride characterize ground \r\nwaters affected by drainage from oil fields. Extensive fracture and dissolution \r\nof the Permian limestones facilitated pollution of ground water by oil-field \r\nbrine and migration of the polluted water into adjacent areas. Ground water \r\ncontaining more than 1,000 mg/o=l (milligrams per liter) dissolved solids .and \r\nmore than 100 mg/o=l chloride is common near oil fields but is exceptional \r\nelsewhere.\r\nThe concentration of nitrate in about 25 percent of the sampled well waters \r\nexceeded the recommended maximum for drinking water. High concentrations \r\nof nitrate generally were associated with shallow aquifers, local sources of \r\norganic pollution, and stagnation. \r\nSodium and chloride are the principle ionic constituents of oil-field brine but \r\nare minor constituents of natural surface waters or shallow ground water in the \r\nbasin. The ratios of the concentrations of sodium to chloride in brine from \r\ndifferent oil fields varied within a narrow range from a mean of 0.52. Concentrations of chloride exceeding 50 mg/o=l in streamflow and 100 mg/l in ground \r\nwater generally signified the presence of oil-field brine if the sodium-chloride \r\nratios were less than 0.60. Higher sodium-chloride ratios characterized relatively rare occurrences of high concentrations of the ions that might have \r\noriginated in evaporite minerals or in sewage. \r\nThe concentration of chloride during low flow of the major streams generally \r\nincreased, and the sodium-chloride ratio decreased, in a downstream direction from about 0.65 near the headwaters to about 0.51, which is characteristic of oil-field brine. The changes were most abrupt where polluted ground-water effluent augmented low streamflow adjacent to old oil fields. With increased direct runoff, the sodium-chloride ratio normally increased, and these ions constituted a smaller percentage of the dissolved-solids load. \r\n\r\nAnnual runoff .decreased progressively from above normal to below normal during water years 1962-64. Higher concentrations .of the ions in streamflow persisted for longer periods during the periods of low runoff","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1982","usgsCitation":"Leonard, R., 1972, Chemical quality of water in the Walnut River basin, south-central Kansas: U.S. Geological Survey Water Supply Paper 1982, viii, 113 p. :ill., maps (3 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1982.","productDescription":"viii, 113 p. :ill., maps (3 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":138319,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1982/report-thumb.jpg"},{"id":27685,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1982/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":247111,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1982/plate-1.pdf","size":"8555","linkFileType":{"id":1,"text":"pdf"}},{"id":247112,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1982/plate-2.pdf","size":"4237","linkFileType":{"id":1,"text":"pdf"}},{"id":247113,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1982/plate-3.pdf","size":"5398","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dee4b07f02db5e3209","contributors":{"authors":[{"text":"Leonard, Robert B.","contributorId":14407,"corporation":false,"usgs":true,"family":"Leonard","given":"Robert B.","affiliations":[],"preferred":false,"id":144688,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1144,"text":"wsp1757M - 1972 - Significance of ground-water chemistry in performance of North Sahara Tube wells in Algeria and Tunisia","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1757M","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1757","chapter":"M","title":"Significance of ground-water chemistry in performance of North Sahara Tube wells in Algeria and Tunisia","docAbstract":"Nine ground-water samples from the principal shallow and deep North Sahara aquifers of Algeria and Tunisia were examined to determine the relation of their chemical composition to corrosion and mineral encrustation thought to be contributing to observed decline in well capacities within a UNESCO/UNDP Special Fund Project area. Although the shallow and deep waters differ significantly in certain quality factors, all are sulfochloride types with corrosion potentials ranging from moderate to extreme. None appear to be sufficiently supersaturated with troublesome mineral species to cause rapid or severe encrustation of filter pipes or other well parts. However, calcium carbonate encrustation of deep-well cooling towers and related irrigation pipes can be expected because of loss of carbon dioxide and water during evaporative cooling. \r\n\r\nCorrosion products, particularly iron sulfide, can be expected to deposit in wells producing waters from the deep aquifers. This could reduce filterpipe openings and increase casing roughness sufficiently to cause significant reduction in well capacity. It seems likely, however, that normal pressure reduction due to exploitation of the artesian systems is a more important control of well performance. If troublesome corrosion and related encrustation are confirmed by downhole inspection, use of corrosion-resisting materials, such as fiber-glass casing and saw-slotted filter pipe (shallow wells only), or stainless-steel screen, will minimize the effects of the waters represented by these samples. A combination of corrosion-resisting stainless steel filter pipe electrically insulated from the casing with a nonconductive spacer and cathodic protection will minimize external corrosion of steel casing, if this is found to be a problem. However, such installations are difficult to make in very deep wells and difficult to control in remote areas. Both the shallow waters and the deep waters examined in this study will tend to cause soil salinization because their salt contents are relatively high, and both have sodium absorption ratios which are unfavorable to sodium-sensitive soils and vegetation. Proper drainage and soil treatment are the only means of overcoming these problems during irrigation.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1757M","usgsCitation":"Clarke, F., and Jones, B.F., 1972, Significance of ground-water chemistry in performance of North Sahara Tube wells in Algeria and Tunisia: U.S. Geological Survey Water Supply Paper 1757, vi, M1-M39 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1757M.","productDescription":"vi, M1-M39 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":137623,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757m/report-thumb.jpg"},{"id":25925,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757m/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f9e4b07f02db5f3ccc","contributors":{"authors":[{"text":"Clarke, Frank Eldridge","contributorId":107255,"corporation":false,"usgs":true,"family":"Clarke","given":"Frank Eldridge","affiliations":[],"preferred":false,"id":143252,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jones, Blair F. bfjones@usgs.gov","contributorId":2784,"corporation":false,"usgs":true,"family":"Jones","given":"Blair","email":"bfjones@usgs.gov","middleInitial":"F.","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":true,"id":143251,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2557,"text":"wsp2009A - 1972 - Runoff characteristics of California streams","interactions":[],"lastModifiedDate":"2012-02-02T00:05:29","indexId":"wsp2009A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"A","title":"Runoff characteristics of California streams","docAbstract":"California streams exhibit a wide range of runoff characteristics that are related to the climatologic, topographic, and geologic characteristics of the basins they drain. The annual volume of runoff of a stream, expressed in inches, may be large or small, and daily discharge rates may be highly variable or relatively steady. The bulk of the annual runoff may be storm runoff, or snowmelt runoff, or a combination of both. The streamflow may be ephemeral, intermittent, or perennial; if perennial, base flow may be well sustained or poorly sustained. In this report the various runoff characteristics are identified by numerical index values. They are shown to be related generally to mean annual precipitation, altitude, latitude, and location with respect to the 11 geomorphic provinces in the California Region. \r\n\r\nWith respect to mean annual precipitation on the watershed, streamflow is generally (1) ephemeral if the mean annual precipitation is less than 10 inches, (2) intermittent if the mean annual precipitation is between 10 and 40 inches, and (3) perennial if the mean annual precipitation is more than 40 inches. Departures from those generalizations are associated with (a) the areal variation of such geologic factors as the infiltration and storage capacities of the rocks underlying the watersheds, and (b) the areal variation of evapotranspiration loss as influenced by varying conditions of climate, soil, vegetal cover, and geologic structure. \r\n\r\nLatitude and altitude determine the proportion of the winter precipitation that will be stored for subsequent runoff in the late spring and summer. In general, if a watershed has at least 30 percent of its area above the normal altitude of the snowline on April 1, it will have significant snowmelt runoff. Snowmelt runoff in California is said to be significant if at least 30 percent of the annual runoff occurs during the 4 months, April through July. Storm runoff is said to be predominant if at least 65 percent of the annual runoff occurs during the 6 months, October through March. Base flow (ground-water outflow), as a factor in the regimen of streamflow, is qualified on the basis of the percentage of the mean annual runoff that occurs during the fair-weather months of August and September. If the sum of the August and September runoff exceeds 3.0 percent of the annual runoff, base flow is considered to be well sustained; if the percentage is between 1.5 and 3.0, base flow is considered to be fairly well sustained; if the percentage is less than 1.5, baseflow is considered to be poorly sustained. \r\n\r\nThe characteristics of duration curves of daily streamflow are influenced by the regimen of runoff. The distribution of daily flow is skewed for all streams, but it is more skewed for streams whose flow is predominantly storm runoff than for streams that carry significantly large quantities of snowmelt. Least skewed is the distribution for streams that carry large quantities of base flow. Either of two characteristics of the duration curve may be used as an index of skew--the percentage of time that the mean discharge is equaled or exceeded or the ratio of the median discharge to the mean discharge. As for variability of daily discharge, the variability of storm-runoff streams is greater than that of snowmelt streams, and the lowest values of variability are associated with streams that carry large quantities of base flow. The index of variability used in this study was the ratio of the discharge equaled or exceeded 10 percent of the time to the discharge equaled or exceeded 90 percent of the time. \r\n\r\nThe identification of streamflow characteristics by numerical index figures greatly facilitates comparison of the diverse runoff regimens of streams in the California Region.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp2009A","usgsCitation":"Rantz, S., 1972, Runoff characteristics of California streams: U.S. Geological Survey Water Supply Paper 2009, iv, A 1-A 38 p. :illus. ;24 cm., https://doi.org/10.3133/wsp2009A.","productDescription":"iv, A 1-A 38 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":138636,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2009a/report-thumb.jpg"},{"id":28808,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2009a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28809,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2009a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cee4b07f02db54576a","contributors":{"authors":[{"text":"Rantz, S. E.","contributorId":34106,"corporation":false,"usgs":true,"family":"Rantz","given":"S. E.","affiliations":[],"preferred":false,"id":145392,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":950,"text":"wsp1939C - 1972 - Electrical-analog analysis of the hydrologic system, Tucson basin, southeastern Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1939C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1939","chapter":"C","title":"Electrical-analog analysis of the hydrologic system, Tucson basin, southeastern Arizona","docAbstract":"The water supply for the Tucson basin, Arizona, is derived entirely from ground water. The average annual pumpage for 1962-64 was about 165,000 acre-feet and was greater than the natural rate of ground-water recharge. Water-level declines of as much as 70 feet occurred from spring 1940 to spring 1965 as a result of the overdraft. \r\n\r\nAn electrical-analog model of the hydrologic system was constructed to provide a tool for determining the possible future effects of ground-water management schemes. Basic data required for the simulation of the hydrologic system in the model included periodic water-level measurements, determinations of transmissibility, and pumpage and recharge values. The model was analyzed using steady-state and storage-depletion techniques. The steady state analysis served to determine the average annual recharge to the hydrologic system and to verify the pattern of transmissibility. The steady-state analysis indicated that 97,000 acre-feet of water was entering and leaving the ground-water reservoir annually prior to extensive development. The storage-depletion analysis for 1940-64 was made to verify that the model was a valid analog of the hydrologic system and, therefore, could be used for the prediction of future water-level conditions. The storage-depletion analysis indicated areas where some of the basic-data values and (or) the conceptual design of the hydrologic system used in the model were in error. After all the hydrologic variables simulated in the model had been adjusted, the analog model reasonably simulated the historical field data. Based on the assumption that pumpage and recharge would continue at existing rates and locations, the model was then used to predict water-level conditions in spring 1985. The results of the projection indicate a maximum water-level decline of 140 feet for 1940-84. The predicted overall shapes of the cones of depression will remain about the same as in the historical period, except that a large amount of lateral development will take place in all the cones.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1939C","usgsCitation":"Anderson, T.W., 1972, Electrical-analog analysis of the hydrologic system, Tucson basin, southeastern Arizona: U.S. Geological Survey Water Supply Paper 1939, 1 portfolio (iv, p. illus.) ;24 cm., https://doi.org/10.3133/wsp1939C.","productDescription":"1 portfolio (iv, p. illus.) ;24 cm.","costCenters":[],"links":[{"id":110053,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25165.htm","linkFileType":{"id":5,"text":"html"},"description":"25165"},{"id":138058,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1939c/report-thumb.jpg"},{"id":25455,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25456,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25457,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939c/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25458,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939c/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25459,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939c/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25460,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1939c/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25461,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1939c/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a19e4b07f02db606096","contributors":{"authors":[{"text":"Anderson, T. W.","contributorId":105686,"corporation":false,"usgs":true,"family":"Anderson","given":"T.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":142906,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1786,"text":"wsp1999I - 1972 - Water for cranberry culture in the Cranmoor area of central Wisconsin","interactions":[],"lastModifiedDate":"2015-10-02T13:26:50","indexId":"wsp1999I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1999","chapter":"I","title":"Water for cranberry culture in the Cranmoor area of central Wisconsin","docAbstract":"The Cranmoor area of central Wisconsin is the principal cranberry producing area of the State. Cranberries are grown in only about 2.5 square miles of an 80-square-mile marsh and swamp in the Cranberry Creek basin. Cranberry growers have built reservoirs and ditches throughout 25 square miles of marsh for better management of the area's natural water supply. Additional water is diverted into the basin to supplement the cranberry needs. In the 1966-67 hydrologic budget for Cranberry Creek basin, annual inputs were 27.8 inches of precipitation, 3.8 inches of surface-water diversion into the basin, and 1.1 inches decrease in stored water. Annual outputs were. 20.8 inches of evapotranspiration, 11.7 inches of runoff, and 0.2 inch of groundwater outflow. During the 1966-67 period, precipitation averaged about 3 inches per year below normal. The water used for cranberry culture is almost exclusively surface water. Efficient management of the basin's water supply, plus intermittent diversions of about 100 cubic feet per second from outside the basin, provide cranberry growers with a sufficient quantity of water. Although the quantity of surface water is adequate, the pH (generally 5.7-6.7) is slightly high for optimum use. Dissolved oxygen is slightly low, generally between 4 and 10 milligrams per liter. The water is soft; iron and manganese contents vary seasonally, being high in winter and summer and low in spring. Additional supplies of surface water can be obtained by increasing diversions from outside the basin and by increasing reservoir capacity within the basin. Ground water, although not presently used for cranberries, is available in the central, southern, and eastern parts of the basin, where the thickness of the saturated alluvium exceeds 50 feet. Well yields in these areas might be as much as 1,000 gpm (gallons per minute). Additionally, well yields of as much as 1,000 gpm may be expected from saturated alluvium southeast of Cranberry Creek basin. Where saturated alluvium is less than 50 feet thick, in the northern and western parts of the basin, well yields generally are less than 50 gpm. Ground water is also available from sandstone in the western part of the basin. Where the sandstone is thickest (about 60 ft.), well yields may be as much as 200 gpm. The quality of ground water is similar to that of surface water. The pH of water from the shallow alluvium ranges between 6.0 and 6,6; the pH of water from the deep alluvium is about 7.0. Ground water is soft to moderately hard, 22 to 88 milligrams per liter, and contains excessive amounts of iron and manganese.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1999I","collaboration":"Prepared in cooperation with University Extension-the University of Wisconsin Geological and Natural History Survey","usgsCitation":"Hamilton, L.J., 1972, Water for cranberry culture in the Cranmoor area of central Wisconsin: U.S. Geological Survey Water Supply Paper 1999, Report: iii, 20 p.; 2 Plates: 34.50 x 24.00 inches and 17.00 x 27.00 inches, https://doi.org/10.3133/wsp1999I.","productDescription":"Report: iii, 20 p.; 2 Plates: 34.50 x 24.00 inches and 17.00 x 27.00 inches","numberOfPages":"26","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":138497,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1999i/report-thumb.jpg"},{"id":26922,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999i/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26923,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1999i/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26921,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999i/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","city":"Cranmoor","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.3131103515625,\n 44.50825885600572\n ],\n [\n -90.450439453125,\n 44.308126684886126\n ],\n [\n -90.3570556640625,\n 44.05601169578525\n ],\n [\n -90.164794921875,\n 44.07969327425713\n ],\n [\n -90.02197265625,\n 44.24126379833979\n ],\n [\n -89.9615478515625,\n 44.296332880058706\n ],\n [\n -89.9176025390625,\n 44.37098696297173\n ],\n [\n -89.945068359375,\n 44.46123053905882\n ],\n [\n -90.0164794921875,\n 44.53175879707938\n ],\n [\n -90.142822265625,\n 44.57873024377564\n ],\n [\n -90.3131103515625,\n 44.50825885600572\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48d1e4b07f02db547e08","contributors":{"authors":[{"text":"Hamilton, Louis J.","contributorId":53768,"corporation":false,"usgs":true,"family":"Hamilton","given":"Louis","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":144154,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2791,"text":"wsp1999A - 1972 - Geohydrology of the lower Verdigris River valley between Muskogee and Catoosa, Oklahoma","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1999A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1999","chapter":"A","title":"Geohydrology of the lower Verdigris River valley between Muskogee and Catoosa, Oklahoma","docAbstract":"Alluvium is the principal aquifer along the Verdigris River between Muskogee and Catoosa, Okla. Yields of 1 to 10 gallons of water per minute, adequate for most domestic and stock uses, are available in almost all areas underlain by alluvium. In places where the proportion of gravel to fine material is high, yields ranging from 10 to 30 gallons per minute are possible from large-diameter wells. Terrace deposits yield small amounts of water (1 to 10 gallons per minute), adequate for most domestic and stock uses. \r\n\r\nWater-level fluctuations, in response to seasonal changes in recharge and discharge, range from 1 to 5 feet. Long-term fluctuations, measured as changes in seasonal high or low water levels during 8 years of record, are about 10 feet in the alluvium and less than 5 feet in the terrace deposits. \r\n\r\nRecharge to the alluvium is mainly by precipitation. Recharge maintains groundwater levels above the level of the Verdigris River, which, in turn, is the natural drain of the aquifer. Discharge from the alluvium is by seepage into the river and its tributaries and by evapotranspiration. \r\n\r\nGenerally, the quality of the water in the alluvium and terrace deposits is suitable for domestic, stock, and irrigation uses.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1999A","usgsCitation":"Tanaka, H., 1972, Geohydrology of the lower Verdigris River valley between Muskogee and Catoosa, Oklahoma: U.S. Geological Survey Water Supply Paper 1999, iii, 23 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1999A.","productDescription":"iii, 23 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":138869,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1999a/report-thumb.jpg"},{"id":29275,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29276,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999a/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29277,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1999a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8838","contributors":{"authors":[{"text":"Tanaka, H.H.","contributorId":30610,"corporation":false,"usgs":true,"family":"Tanaka","given":"H.H.","email":"","affiliations":[],"preferred":false,"id":145796,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1120,"text":"wsp2021 - 1972 - Evaluation of yields of wells in consolidated rocks, Virginia to Maine","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp2021","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"2021","title":"Evaluation of yields of wells in consolidated rocks, Virginia to Maine","docAbstract":"In the North Atlantic region, Virginia to Maine, yields of industrial and municipal wells are the most reliable indicators of the water-yielding potential of consolidated rocks. Generally, such wells represent efforts to develop a maximum supply of water, they are 350 to 500 feet deep, and they utilize 60 to 150 feet of drawdown. In multiple-well developments, average yields of wells per 100 feet of drawdown range from less than 75 gallons per minute in the least favorable rocks such as shale or granite gneiss to as much as 300 gallons per minute in limestone. In any one rock type, substantially greater than average sustained yields are possible in structurally deformed areas or in areas where recharge potential is especially favorable.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp2021","usgsCitation":"Cederstrom, D.J., 1972, Evaluation of yields of wells in consolidated rocks, Virginia to Maine: U.S. Geological Survey Water Supply Paper 2021, iv, 38 p. :2 fold. illus. (in pocket) ;24 cm., https://doi.org/10.3133/wsp2021.","productDescription":"iv, 38 p. :2 fold. illus. (in pocket) ;24 cm.","costCenters":[],"links":[{"id":138012,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2021/report-thumb.jpg"},{"id":25883,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2021/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25884,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2021/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25885,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2021/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5f9d4e","contributors":{"authors":[{"text":"Cederstrom, Dagfin John","contributorId":90287,"corporation":false,"usgs":true,"family":"Cederstrom","given":"Dagfin","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":143209,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1636,"text":"wsp2119 - 1972 - Surface water supply of the United States, 1966-70, Part 6, Missouri River basin, v. 4, Missouri River basin below Nebraska City, Nebraska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:14","indexId":"wsp2119","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"2119","title":"Surface water supply of the United States, 1966-70, Part 6, Missouri River basin, v. 4, Missouri River basin below Nebraska City, Nebraska","language":"ENGLISH","publisher":"USGS,","doi":"10.3133/wsp2119","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1972, Surface water supply of the United States, 1966-70, Part 6, Missouri River basin, v. 4, Missouri River basin below Nebraska City, Nebraska: U.S. Geological Survey Water Supply Paper 2119, 901 p. ;23 cm., https://doi.org/10.3133/wsp2119.","productDescription":"901 p. ;23 cm.","costCenters":[],"links":[{"id":137222,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2119/report-thumb.jpg"},{"id":26703,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2119/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af4e4b07f02db691dfc","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":527995,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":939,"text":"wsp1973 - 1972 - Availability of water in Kalamazoo County, southwestern Michigan","interactions":[],"lastModifiedDate":"2016-08-26T13:54:14","indexId":"wsp1973","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1972","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":"1973","title":"Availability of water in Kalamazoo County, southwestern Michigan","docAbstract":"Kalamazoo County comprises an area of 572 square miles in the southwestern part of Michigan. It includes parts of the Kalamazoo, St. Joseph, and Paw Paw River basins, which drain into Lake Michigan. The northern two-thirds of the county is drained by the Kalamazoo River and its tributaries. A small area in the western piart of the county is drained by the Paw Paw River, and the rest, by tributaries of the St. Joseph River. Glacial deposits, containing sand and gravel, form an upper aquifer and a lower aquifer underlying large parts of the county. Areas of high transmissibility and thick saturated deposits are sufficiently localized to be considered as separate ground-water reservoirs having limited areal extent and definite hydrologic boundaries.
Ground-water runoff from the basins constitutes a large part of the streamflow. Hydrograph separation shows that ground-water runoff composed 65 and 73 percent of the discharge of Kalamazoo River at Comstock and 75 and 79 percent of the discharge of Portage River near Vicksburg in 1965 and 1966, respectively. Based on the hydrologic budgets for the same years, ground-water recharge was 9.1 and 9.0 inches in the Kalamazoo River basin and 12.2 and 11.6 inches in the St. Joseph River basin.
Ground-water recharge in the Kalamazoo River basin extrapolated for the 34-year period 1933-66 ranged from 4 to 13 inches and averaged 9 inches. In the St. Joseph River basin average recharge was about 9 inches for the same period.
There is a wide range in runoff in the county. Augusta Creek, Portage Creek near Kalamazoo, and Gourdneck Creek have the highest annual runoff and maintain high yields even during periods of deficient precipitation. Spring Brook also reflects large ground-water contributions to streamflow. Storage in these basins could provide additional water during low flows for municipal and industrial needs.
The primary use of lakes in the county is for recreational and esthetic purposes. Maintaining lake levels is therefore of the utmost importance. Levels at Crooked and Eagle Lakes have been maintained by pumping from lower aquifers. Diversion of water from Gourdneck Creek to West and Austin Lakes has helped in maintaining levels. Several relatively undeveloped lakes could be utilized as reservoirs whose storage could be used to augment streamflow or for water supply.
Water in streams is generally of good chemical quality; however, several streams, including the Kalamazoo River downstream from Kalamazoo, have been degraded by municipal and industrial waste disposal. Water in the lakes is generally of good chemical quality with the exception of Barton Lake, which has been degraded by waste disposal.
There is sufficient surface water available in Kalamazoo County to meet requirements for development of large quantities of water. The total available supply (average discharge of a stream) is about 680 mgd (million gallons per day). The dependable supply (7-day Q2, or average 7-day low flow having a recurrence interval of 2 years) is about 303 mgd. By developing artificial recharge facilities, surface runoff during winter and spring could be utilized to recharge ground-water reservoirs.
Surface-water withdrawal in 1966 was about 58 mgd, of which 33 mgd was withdrawn from the Kalamazoo River. The quantity of water now being withdrawn from the ground and surface sources is small compared to the total that may be obtained in the area through full utilization of these resources.
Mathematical models were used to simulate hydrologic conditions in the ground-water reservoirs and to evaluate maximum drawdowns for periods of little or no recharge. The practical limits of development as determined for the ground-water reservoirs are estimated to be at the following average withdrawal rates: Kalamazoo, 39 .mgd; Schoolcraft, 17 mgd; Kalamazoo-Portage, 24 mgd; and several small reservoirs, 67 mgd. These total 147 mgd. Further development would require additional artificial recharge facilities.
Average ground-water withdrawal in 1966 was about 54 mgd. The Kalamazoo River ground-water reservoir furnished about 28 mgd, the Kalamazoo-Portage ground-water reservoir, about 21 mgd, and the other reservoirs, about 5 mgd. Thus, further development without artificial recharge is estimated to be about 11 mgd in the Kalamazoo River reservoir, 17 mgd in the Schoolcraft reservoir, 62 mgd in the several small reservoirs, and only 3 mgd in the Kalamazoo-Portage reservoir.
The ground water is generally of good chemical quality and is suitable for most uses; however, it is Usually very hard and may contain objectionable amounts of iron. Some deterioration of water quality- has .been observed in several areas because of seepage from stockpiles of industrial minerals.
The presence of many inland lakes, streams having high ground-water runoff, and, in places, relatively undeveloped ground-water reservoirs provides -flexibility in water management.
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