Within the Mesabi-Vermilion Iron Range area, water of good quality is available from the Biwabik Iron-Formation, from stratified drift, and from lakes and streams. About 700 bgy (billion gallons a year) leaves the area as surface water, of which about one-third comes from ground water.
\nLeached, oxidized, and fractured parts of the Biwabik Iron-Formation yield as much as 1,000 gpm (gallons per minute) to wells. Much of the permeable stratified drift within the area underlies the Ice-Contact region and the Horainal and Ice-Contact region, and several wells drilled in drift have been pumped at rates of more than 1,000 gpm.
\nParts of three major drainage basins lie within the area, and lakes compose about 5 percent of the area. Low-flow and flood-frequency data have been compiled for many of the streams. Large quantities of surface water are available from the Border-Lakes region and the Morainal and Ice-Contact region.
\nThe quality of ground water from the Biwabik Iron-Formation and from the drift is similar. The water is generally moderately siliceous, hard or very hard, and contains much iron and manganese. Surface water is generally soft, contains much iron, and is highly colored.
\nLarge uses of water in the area include: taconite processing (50 bgy), wash-ore processing (19 bgy), power plants (63 bgy), municipal water supplies (3 bgy) and paper processing (1 bgy). Optimum development of the water resources might be achieved by using streamflow in the spring and stunner and ground-water and surface-water storage in the fall and winter.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1759A","collaboration":"Prepared in cooperation with the Minnesota Department of Iron Range Resources and Rehabilitation","usgsCitation":"Cotter, R.D., Young, H.L., Petri, L.R., and Prior, C.H., 1965, Ground and surface water in the Mesabi and Vermilion Iron Range area, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 1759, Document: iv, 35 p.; 1 Plate: 23.00 x 17.00 inches, https://doi.org/10.3133/wsp1759A.","productDescription":"Document: iv, 35 p.; 1 Plate: 23.00 x 17.00 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":400746,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24933.htm"},{"id":26060,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1759a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26059,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1759a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137940,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1759a/report-thumb.jpg"}],"scale":"303000","country":"United States","state":"Minnesota","otherGeospatial":"Mesabi and Vermilion Iron Range area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.75,\n 48\n ],\n [\n -93.75,\n 47.089\n ],\n [\n -91.582,\n 47.089\n ],\n [\n -91.582,\n 48\n ],\n [\n -93.75,\n 48\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab1e4b07f02db66eaed","contributors":{"authors":[{"text":"Cotter, R. D.","contributorId":89874,"corporation":false,"usgs":true,"family":"Cotter","given":"R.","email":"","middleInitial":"D.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":143330,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Young, H. L.","contributorId":23922,"corporation":false,"usgs":true,"family":"Young","given":"H.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143327,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143328,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prior, C. H.","contributorId":57827,"corporation":false,"usgs":true,"family":"Prior","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143329,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1062,"text":"wsp1790A - 1965 - Floods of March-April 1960 in Eastern Nebraska and adjacent states","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1790A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1965","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":"1790","chapter":"A","title":"Floods of March-April 1960 in Eastern Nebraska and adjacent states","docAbstract":"Snowmelt floods, record breaking on many streams and outstanding in terms of total area affected and runoff volumes generated, occurred in late March and early April 1960 on Missouri River tributaries in adjacent parts of six states. In order of area affected, the States are Nebraska, South Dakota, Iowa, Kansas, Minnesota, and Missouri. \r\n\r\nFive lives were lost, and the estimated damage was $14 million. Main-stem reservoirs kept Missouri River stages substantially below potential unregulated levels. Without regulation by reservoirs, the stage at Sioux City and Omaha would have been about 9 feet higher than it was and the damage would have been many millions of dollars more than actually occurred. \r\n\r\nThe floods were caused by rapid melting of an extensive snow cover of unusual depth and water equivalent, augmented by light to moderate rains. Temperatures almost continuously below normal, beginning in late December and culminating in record lows at many places during the first half of March, resulted in the retention of record snow accumulations, much later and much farther south than normal. The snowfall in eastern Nebraska from December 27 to March 26 was about twice the annual average. The excessive snowfall and below-normal temperatures produced a record-breaking 75-day period of continuous snow cover at Omaha. \r\n\r\nA rapidly rising, eastward-moving temperature pattern late in March, in combination with an easterly orientation of many Nebraska streams, tended to magnify flood peaks. The rapid temperature rise started about March 18 in western Nebraska but not until March 26 in the eastern part of the State. As a consequence, flood discharges from the headwaters, often bearing heavy ice floes, arrived in the lower reaches simultaneously with or even ahead of the breakup of the unusually heavy ice cover and caused serious jamming. Comparisons of the peak discharges of the 1960 snowmelt floods with those of previous floods reveal several interesting facts. Peak discharges on the Missouri main stem were appreciably less than those in several other years, largely because of effective reservoir control of upstream runoff, but, many tributaries throughout the report area had maximum discharges for their periods of record. Particularly significant are comparisons at some stations for which historical flood data were available. For example, the peak discharge of the Platte River at Louisville, Nebr., was the greatest since at least 1881, and the peak on the Elkhorn River at Waterloo, Nebr., was the greatest snowmelt flood since at least 1912, although it was less than half of the rain peak of June 12, 1944. \r\n\r\nFollowing a characteristic pattern for snowmelt floods, the peaks on the smaller streams generally were not unusual, but the cumulative effect of widespread high runoff throughout the stream systems caused higher and more outstanding peaks in the larger basins. Peaks due to local rains of high intensity often are more significant for small areas. \r\n\r\nSnowmelt floods occur less frequently than rainfall floods in most basins of this flood area.. Studies made for this report show that an average of only about one out of every four maximum annual flood discharges in the report area results primarily from snowmelt. But for streams flowing from north to south in South Dakota and Iowa, the ratio of snowmelt peaks to rainfall peaks is higher. \r\n\r\nComparisons of 1960 flood volumes with those for previous floods are even more striking than peak-discharge comparisons. Flood volumes at eight selected stations for the maximum 20-day period during March and April 1960 exceeded all previous 20-day volumes with only one exception; the ratios ranged from 3.11 for Vermillion River near Wakonda, S. Dak., to 0.93 for Elkhorn River at Waterloo, Nebr. The ratio of the 20-day volume to the 1960 annual runoff for the same group of stations ranged from 20 percent at Niobrara River near Spencer, Nebr., to 74 percent on the Vermillion River. For the lat","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey ;","doi":"10.3133/wsp1790A","usgsCitation":"Brice, H., and West, R., 1965, Floods of March-April 1960 in Eastern Nebraska and adjacent states: U.S. Geological Survey Water Supply Paper 1790, v, 144 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1790A.","productDescription":"v, 144 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138100,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1790a/report-thumb.jpg"},{"id":25740,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1790a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25741,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1790a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d9e4b07f02db5df9c2","contributors":{"authors":[{"text":"Brice, H.D.","contributorId":41406,"corporation":false,"usgs":true,"family":"Brice","given":"H.D.","email":"","affiliations":[],"preferred":false,"id":143112,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"West, R.E.","contributorId":27031,"corporation":false,"usgs":true,"family":"West","given":"R.E.","email":"","affiliations":[],"preferred":false,"id":143111,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2897,"text":"wsp1811 - 1965 - Hydrology of the Little Plover River basin, Portage County, Wisconsin, and the effects of water resource development","interactions":[],"lastModifiedDate":"2023-04-13T20:54:27.826245","indexId":"wsp1811","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","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":"1811","title":"Hydrology of the Little Plover River basin, Portage County, Wisconsin, and the effects of water resource development","docAbstract":"The Little Plover River basin is in the sand-plain area of central Wisconsin. The basin and the surrounding sand-plain area provide a good fish and wildlife habitat and is a popular locale for sport fishing. Good yields may be obtained in the area from irrigated crops, and the irrigated acreage has been increasing rapidly in recent years. Sportsmen and conservationists are concerned about the effects of increased development of the water resources on the streams as trout habitat. In the past, many political and legal conflicts among water users have arisen from erroneous opinions as to the behavior of water. Many of these conflicts would be diminished or eliminated if the participants were cognizant of fundamental hydrologic principles.
This study was made to demonstrate the extent and nature of the interrelation of ground water and surface water and the fundamental hydrologic principles governing water movement. The study was also made to determine the hydrologic changes that might occur following development, to provide information that might be used as a basis for planning water development, and for drafting legislation that recognizes the relation between ground water and surface water.
Water has been developed in the Little Plover River basin for industry, for domestic and stock supplies, and for irrigation. Irrigated acreage is increasing in the area, and the use of water for irrigation may alter the hydrology of the basin somewhat. About 4,000-4,500 acres of land within the basin, or 50-60 percent of the basin area, is suitable for irrigated farming, but probably no more than 2,500 acres will be under irrigation in any one year, unless present crop-rotation practices are changed.
Most of the Little Plover River basin is underlain by from 40 to 100 feet of glacial outwash consisting of highly permeable sand and gravel. The glacial outwash is the main aquifer in the area and is capable of yielding large quantities of water to wells. An aquifer test in the area indicated that the coefficient of transmissibility of the glacial outwash is about 140,000 gallons per day per foot. The specific yield of the outwash is about 20 percent, as determined from water-level and streamfiow data. Morainal deposits occur locally with the glacial outwash. These deposits transmit water readily and do not form barriers to ground water in the outwash. Relatively impermeable crystalline rocks underlie the glacial deposits, and a sandstone ridge of low permeability impedes the movement of ground water from the basin by underflow.
The glacial outwash and morainal deposits are recharged by infiltration of 9-10 inches of the 31 inches of precipitation that falls on the area in an average year. If it is not withdrawn by wells for consumptive use or by phreatophytes, water that infiltrates the sand and gravel discharges later into the Little Plover River. This ground-water discharge constitutes 90-95 percent of the total flow of the Little Plover River.
Annual evapotranspiration varies considerably, but generally ranges from 2 to 8 inches less than the potential evapotranspiration of 24 inches. Consumptive use of irrigation water averages about 4 inches per year. Most of the water pumped from wells otherwise would be discharged to the stream, and consumptive use of irrigation water will deplete streamflow by the amount of evapotranspiration.
Pumping wells have little effect on the water level in the highly permeable sand and gravel. Significant interference between wells would occur only if large capacity wells were within a few tens of feet of each other.
Ground water and surface water are closely interrelated in the sand-plain area and ground-water withdrawals near the Little Plover River may cause a measurable streamflow depletion. In a test, a well that was pumping about 1,120 gpm (gallons per minute) and that was 300 feet from the stream derived about 30 percent of its flow from the stream after 3 days of pumping.
For this study, the effects of increased ground-water development were evaluated from a hypothetical development schedule, for which it was assumed that 500 acres were irrigated the first year and that an additional 50 acres were irrigated in each succeeding year for 10 years. It also was assumed that the average annual consumptive-use requirement for irrigation water would be one- third of an acre-foot per acre. Calculations indicate that the maximum monthly rate of depletion due to the consumptive use of 4 inches of ground water per year on 500 acres would be about 0.4 cfs (cubic feet per second) the first year and 0.5 cfs after 10 years of pumping. Other computations indicate that the maximum monthly rate of depletion due to irrigating 500 acres the first year and 50 additional acres each year for 10 years would be about 0.8 cfs. Maximum depletion would occur during the summer months, concurrent with the irrigation withdrawals.
Because of the close interrelation between ground and surface water, surface- water withdrawals will cause an increased inflow of ground water to the stream and a decline in ground-water levels near the stream. These effects were demonstrated by pumping from the stream. After 29 hours of pumping, a depletion of 1,120 gpm at a site 7,000 feet downstream was about 200 gpm less than the diversion at the pump. Most of the 200 gpm was supplied from the stream-banks, and ground-water levels near the stream declined as much as 0.3 foot. Computations indicated that ground-water inflow, following a streamflow diver- sion that lowered the stage 0.15 foot, would be 0.14 cfs after 5 days and 0.06 cfs after 30 days.
The demonstration of the quantitative relation between ground water and surface water, as given by this study, should provide a sound basis for planning water development to minimize conflicts of interest. The demonstrations also should provide a basis for drafting legislation that recognizes the interrelation of ground water and surface water.
Because the geology and the hydrology are relatively uniform throughout the sand plains, many of the methods and hydrologic values determined for this detailed study of the Little Plover River basin may be applied to other basins in the sand-plain area.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1811","collaboration":"Prepared in cooperation with the Wisconsin Conservation Department and the University of Wisconsin Geological and Natural History Survey","usgsCitation":"Weeks, E.P., Erickson, D.W., and Holt, C.L., 1965, Hydrology of the Little Plover River basin, Portage County, Wisconsin, and the effects of water resource development: U.S. Geological Survey Water Supply Paper 1811, Report: v, 78 p.; 6 Plates: 21.00 x 18.01 inches or smaller, https://doi.org/10.3133/wsp1811.","productDescription":"Report: v, 78 p.; 6 Plates: 21.00 x 18.01 inches or smaller","numberOfPages":"85","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":415734,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25017.htm","linkFileType":{"id":5,"text":"html"}},{"id":29561,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1811/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29559,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1811/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29558,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1811/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29562,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1811/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29560,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1811/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29563,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1811/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138378,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1811/report-thumb.jpg"},{"id":29557,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1811/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Portage County","otherGeospatial":"Little Plover River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -89.589,\n 44.554\n ],\n [\n -89.589,\n 44.404\n ],\n [\n -89.367,\n 44.404\n ],\n [\n -89.367,\n 44.554\n ],\n [\n -89.589,\n 44.554\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdc0c","contributors":{"authors":[{"text":"Weeks, Edwin P. epweeks@usgs.gov","contributorId":2576,"corporation":false,"usgs":true,"family":"Weeks","given":"Edwin","email":"epweeks@usgs.gov","middleInitial":"P.","affiliations":[],"preferred":true,"id":145973,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Erickson, Donald W.","contributorId":34900,"corporation":false,"usgs":true,"family":"Erickson","given":"Donald","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":145974,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Holt, Charles Lee Roy Jr.","contributorId":77913,"corporation":false,"usgs":true,"family":"Holt","given":"Charles","suffix":"Jr.","email":"","middleInitial":"Lee Roy","affiliations":[],"preferred":false,"id":145975,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70176114,"text":"70176114 - 1965 - Surface water records of Texas, 1964","interactions":[],"lastModifiedDate":"2017-04-19T10:37:54","indexId":"70176114","displayToPublicDate":"1965-01-01T00:00:00","publicationYear":"1965","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":5196,"text":"Water Data Report","active":true,"publicationSubtype":{"id":6}},"title":"Surface water records of Texas, 1964","docAbstract":"The surface-water records for the 1964 water year for gaging stations, partial-record stations, miscellaneous sites, and base-flow studies within the State of Texas are given in this report. For convenience there are also included records for a few pertinent gaging stations in bordering States. The records were collected and computed by the Water Resources Division of the U. S. Geological Survey, under the direction of Trigg Twichell, district chief, Water Resources Division.
Through September 30, 1960, the records of discharge and stage of streams and contents and stage of lakes or reservoirs were published in an annual series of U.S. Geological Survey water supply papers, entitled \"Surface Water Supply of the United States.\" Since 1951 there have been 20 volumes in the series; each volume covered an area whose boundaries coincided with those of certain natural drainage areas. The records in Texas were contained in Parts 7 and 8 of that series.
Beginning with the 1961 water year, streamflow records and related data have been released by the Geological Survey in annual reports on a State-boundary basis. Distribution of these basic-data reports is limited and primarily for local needs. Records will be published in Geological Survey water-supply papers at 5-year intervals.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/70176114","collaboration":"Prepared in cooperation with the Texas Water Commission, Pecos River Commission, Sabine River Compact Administration, City of Dallas, City of Houston, U.S. Army Corps of Engineers, U.S. Soil Conservation Service, U.S. Public Health Service, and U.S. Bureau of Reclamation","usgsCitation":"U.S. Geological Survey, 1965, Surface water records of Texas, 1964: Water Data Report, xiv, 479 p., https://doi.org/10.3133/70176114.","productDescription":"xiv, 479 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":327888,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70176114/report-thumb.jpg"},{"id":339086,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70176114/report.pdf","text":"Report","size":"234.10 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57c1683ee4b0f2f0ceb90861","contributors":{"authors":[{"text":"U.S. Geological Survey","contributorId":128037,"corporation":true,"usgs":false,"organization":"U.S. Geological Survey","id":647150,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":57732,"text":"ofr64169 - 1964 - Ground-water levels in observation wells in Oklahoma, 1961-62","interactions":[],"lastModifiedDate":"2018-11-16T09:34:27","indexId":"ofr64169","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"64-169","title":"Ground-water levels in observation wells in Oklahoma, 1961-62","docAbstract":"The investigation of the ground-water resources of Oklahoma by the U. S. Geological Survey in cooperation with the Oklahoma Water Resources Board includes a continuing program to collect records of water levels in selected observation wells on a systematic basis. These water-level records: (1) provide an index to available ground-water supplies; (2) facilitate the prediction of trends in water levels that will indicate likely changes in storage; (3) aid in the prediction of the base flow of streams; (4) provide information for use in basic research; (5) provide long-term continuous records of fluctuations of water levels in representative wells; and (6) serve as a framework to which other types of hydrologic data may be related.
Prior to 1956, measurements of water levels in observation wells in Oklahoma were included in water-supply papers published annually by the U. S. Geological Survey (table 1). Beginning with the 1956 calendar year, however, Geological Survey water-level reports will contain only records of a selected network of observation wells, and will be published at 5-year intervals. The first of this series, for the 1956-59 period, was published in 1962.
This report has been prepared primarily to present water-level records of wells not included in the Federal network. However, for the sake of completeness it includes water-level records of Federal wells that either have been or will be published in Water-Supply Papers since 1955. This report, which contains water-level records for the 2-year period (1961-62), is the second of a series presenting water-level records for all permanent observation wells in Oklahoma. The first report, published in 1963, contains water-level records for the 5-year period (1956-60).
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Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"493","title":"Magnitude and frequency of floods in Alaska south of the Yukon River","docAbstract":"This report presents a method for evaluating the magnitude and frequency of floods on the basis of the analysis of flood records. One composite frequency curve is applied to the entire study region. This curve relates floods of various magnitudes at any site within the region to probable recurrence intervals (from 1.1 to 50 years) for those floods. Flood magnitudes are reduced to dimensionless form by expressing them as a ratio to mean annual flood. Magnitudes of mean annual floods vary with the flood-producing characteristics of stream basins. On the basis of the limited data available, drainage-area size is found to be the only significant factor affecting the magnitude of the mean annual flood. Trial and error groupings of gaging-station records show that the region can be split into three hydrologic areas: one curve defines the relation within each area between mean annual flood and drainage area. These three curves in combination with the composite flood-frequency curve permit, for natural-flow conditions at any site, the determination of flood magnitude for a given recurrence interval, or the determination of recurrence interval for a flood of known magnitude.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/cir493","collaboration":"Prepared in cooperation with the Alaska State Highway Department and the U.S. Bureau of Public Roads","usgsCitation":"Berwick, V.K., Childers, J.M., and Kuentzel, M., 1964, Magnitude and frequency of floods in Alaska south of the Yukon River: U.S. Geological Survey Circular 493, Report: iii, 15 p.; 1 Map: 19.27 x 16.80 inches, https://doi.org/10.3133/cir493.","productDescription":"Report: iii, 15 p.; 1 Map: 19.27 x 16.80 inches","numberOfPages":"19","costCenters":[],"links":[{"id":122497,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/0493/report-thumb.jpg"},{"id":31254,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/0493/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271065,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/0493/plate-1.pdf"}],"country":"United States","state":"Alaska","otherGeospatial":"Yukon River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ 172.45,51.21 ], [ 172.45,71.39 ], [ -129.99,71.39 ], [ -129.99,51.21 ], [ 172.45,51.21 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649542","contributors":{"authors":[{"text":"Berwick, Vernon Kenneth","contributorId":50806,"corporation":false,"usgs":true,"family":"Berwick","given":"Vernon","email":"","middleInitial":"Kenneth","affiliations":[],"preferred":false,"id":148292,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Childers, Joseph M.","contributorId":14379,"corporation":false,"usgs":true,"family":"Childers","given":"Joseph","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":148291,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kuentzel, M.A.","contributorId":84248,"corporation":false,"usgs":true,"family":"Kuentzel","given":"M.A.","email":"","affiliations":[],"preferred":false,"id":148293,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":52439,"text":"ofr64167 - 1964 - Flow characteristics of Wisconsin streams: Flow-duration, Hhgh-flow, and low-flow tables for selected streams through water-year 1960","interactions":[],"lastModifiedDate":"2015-10-13T12:41:03","indexId":"ofr64167","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"64-167","title":"Flow characteristics of Wisconsin streams: Flow-duration, Hhgh-flow, and low-flow tables for selected streams through water-year 1960","docAbstract":"The collection of data on the flow of rivers in Wisconsin started on a continuing basis in 1913. A few streamflow records were started in the late 1800's, one as early as 1888 (Chippewa River at Chippewa Falls). Much of the work has been done under cooperative arrangements between the U.S. Geological Survey and various State and Federal agencies. These data have been published in the form of daily discharge tables, and monthly and yearly summaries.
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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d8e4b07f02db5df625","contributors":{"authors":[{"text":"Young, K.B.","contributorId":77997,"corporation":false,"usgs":true,"family":"Young","given":"K.B.","email":"","affiliations":[],"preferred":false,"id":245345,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1233,"text":"wsp1499H - 1964 - Water resources of the Hartford-New Britain area, Connecticut","interactions":[],"lastModifiedDate":"2022-12-19T21:17:22.931346","indexId":"wsp1499H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1499","chapter":"H","title":"Water resources of the Hartford-New Britain area, Connecticut","docAbstract":"The Hartford-New Britain area includes the metropolitan areas of Hartford and New Britain and parts of several adjoining towns. Water used in the area is withdrawn from the principal streams and aquifers at an average rate of 463.5 mgd (million gallons per day). Sufficient water is available from these sources to meet present requirements and those for many years to come, although local shortages may develop in some areas as the result of problems of distribution and treatment. About 98 percent of all water used in 1957 was from surface sources. More than 425 mgd was required by industry, and about 23 mgd was for domestic water supply. The Farmington River upstream from Collinsville is the chief source of water for public supply in the Hartford-New Britain area, whereas the Connecticut River is the chief source of water for industry. An average of about 40 mgd is withdrawn from the upper Farmington River for public supply, and about 404 mgd is withdrawn by industry from the Connecticut River for nonconsumptive use and returned directly to the stream.
The Connecticut River is the source of the largest quantity of water in the area. The flow of the stream at Thompsonville may be expected to equal or exceed about 2,000 mgd 95 percent of the time, and the flow should not be less than this amount for periods longer than 12 days. The flow below Thompsonville is increased by additions from the Scantic, Farmington, Park, and Hockanum Rivers and from numerous smaller tributary streams. The available streamflow data for the aforementioned rivers have been summarized graphically in the report.
The chemical quality of water in the Connecticut River is good, except for short periods when the iron concentration is high. In addition to the removal of iron some other treatment may be necessary if water from the Connecticut River is used for special purposes. The chemical quality of the tributary streams is good, except the quality of the Park River, which is poor. Thus the Connecticut River in the vicinity of Hartford offers an almost unlimited source of water of good chemical quality to the Hartford, New Britain area. The Connecticut River and many of its tributaries, however, are polluted to some degree, and the cost of treatment for pollution and of delivery of water to the area presents an economic problem in the further development of these sources.
The Hartford-New Britain area in the vicinity of Hartford has been plagued by floods since the time of its settlement. Most of the damage to property and loss of life in the Hartford area has been caused by flooding of the Connecticut and Park Rivers. Floods have occurred on the Connecticut River and its tributaries in every month of the year, but the most severe floods occur in the spring and fall. The most devastating flood on the Connecticut River occurred on March 21, 1986, when the stage at Hartford reached 37.0 feet above mean sea level. The maximum flood on the Park River occurred on August 19, 1955, when the stage reached 43.5 feet above mean sea level. Floods on the other tributaries have been frequent and some have been large, but damage has not been as great because the streams flow mostly through rural areas.
Small to moderate supplies of water suitable for domestic use and for small municipalities and industries are available from wells in the Hartford-New Britain area. Moderate supplies are obtainable from five definable sand-and-gravel aquifers and from widespread consolidated sedimentary rocks. Yields to individual wells range from 15 to 400 gpm (gallons per minute) for wells penetrating sand and gravel and from 1 to 578 gpm for wells penetrating consolidated sedimentary rocks. Sand and gravel deposits bordering the Connecticut River downstream from Rocky Hill afford the greatest potential for the development of large supplies of ground water. Small supplies ranging from 1 to 40 gpm are obtainable from glacial till and from consolidated crystalline rocks.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1499H","usgsCitation":"Cushman, R.V., Tanski, D., and Thomas, M.P., 1964, Water resources of the Hartford-New Britain area, Connecticut: U.S. Geological Survey Water Supply Paper 1499, Report: vi, 96 p.; 2 Plates: 24.00 × 27.53 inches and 24.50 × 31.32 inches, https://doi.org/10.3133/wsp1499H.","productDescription":"Report: vi, 96 p.; 2 Plates: 24.00 × 27.53 inches and 24.50 × 31.32 inches","costCenters":[],"links":[{"id":138071,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499h/report-thumb.jpg"},{"id":26160,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499h/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26158,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499h/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26159,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499h/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":410735,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24444.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Connecticut","city":"Hartford, New Britain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -72.5670,\n 41.875\n ],\n [\n -72.875,\n 41.875\n ],\n [\n -72.875,\n 41.625\n ],\n [\n -72.5670,\n 41.625\n ],\n [\n -72.5670,\n 41.875\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49efe4b07f02db5eda7b","contributors":{"authors":[{"text":"Cushman, Robert Vittum","contributorId":96661,"corporation":false,"usgs":true,"family":"Cushman","given":"Robert","email":"","middleInitial":"Vittum","affiliations":[],"preferred":false,"id":143414,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tanski, D.","contributorId":83385,"corporation":false,"usgs":true,"family":"Tanski","given":"D.","email":"","affiliations":[],"preferred":false,"id":143413,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, M. P.","contributorId":62574,"corporation":false,"usgs":true,"family":"Thomas","given":"M.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":143412,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1947,"text":"wsp1748 - 1964 - Apparatus and techniques for measuring bedload","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1748","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1748","title":"Apparatus and techniques for measuring bedload","docAbstract":"The need for accurate determinations of the total sediment discharge of particles of bedload size has prompted this investigation of available and possible measuring apparatus and procedures. The accuracy of measurements of sediment discharge made with trap-type samplers is affected by the variability of sampler efficiency, by the oscillatory variation of bedload discharge, and by sampler placement. Equations that were developed for determining total discharge from measured bedioad discharge and measured suspended-sediment discharge are simplest if the bedload apparatus measures only the true bedload. \r\n\r\nEarly bedload samplers are generally unsatisfactory. Recently developed or suggested apparatus include various improved samplers of the pressure-difference type, a pumping sampler, a magnetic sampler, acoustical instruments that measure the magnitude of the sound of particle collisions, an ultrasonic bedload sampler designed to measure and integrate electronically the concentration and velocity, and a tiltmeter designed to measure the total sediment discharge from the ground tilt that results from the passage of flow. All the pressure-difference samplers are improvements over early samplers, but none are void of the inherent shortcomings of trap-type apparatus; probably the Sphinx (Dutch) and VUV (Hungarian) samplers are the most satisfactory. The acoustical instruments are capable of measuring only the relative discharge. The ultrasonic sampler and the tiltmeter are not adequate without further development. \r\n\r\nSome new possible apparatus and means for measuring or aiding in measuring bedload discharge are small pit samplers, ultrasonic sounders, pressure transducers, and photography. A small pit sampler for measuring bedload discharge was designed to provide self-placement and portability ; however, its practicability and efficiency are undetermined. Exploratory films show that by using slowmotion photography the discharge of particles larger than about pea size can be determined provided the flow is clear; however, photography generally is not practical. Ultrasonic sounders provide continuous and accurate data on bed configuration and dune movement for use in equations that were developed for computing the bedload discharge. Computations with the equations indicate that the interpretation of the sounding data needs further study. Pressure transducers placed beneath the bed surface possibly can be used to provide information on dune movement; however, their installation would be difficult. The time required for collecting data on bed configuration and dune movement throughout a cross section could be substantially reduced by using several transducers simultaneously in conjunction with an ultrasonic sounder. A modified ultrasonic sounder that provides information on the shape and velocity of large particles and a method for determining the discharge of such particles were proposed; the method seems most feasible for particles of high sphericity.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1748","usgsCitation":"Hubbell, D.W., 1964, Apparatus and techniques for measuring bedload: U.S. Geological Survey Water Supply Paper 1748, v, 74 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1748.","productDescription":"v, 74 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":27278,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1748/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138418,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1748/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4883e4b07f02db51824d","contributors":{"authors":[{"text":"Hubbell, David Wellington","contributorId":88330,"corporation":false,"usgs":true,"family":"Hubbell","given":"David","email":"","middleInitial":"Wellington","affiliations":[],"preferred":false,"id":144417,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1122,"text":"wsp1773 - 1964 - Geology and ground-water resources of the Anchorage area, Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1773","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1773","title":"Geology and ground-water resources of the Anchorage area, Alaska","docAbstract":"The Anchorage area, at the head of Cook Inlet in south-central Alaska, \r\noccupies 150 square miles of a glaciated lowland and lies between two estuaries and the Chugach Mountains. Two military bases are in the area; \r\nAnchorage is the largest city in Alaska and the chief transportation center \r\nfor this part of the State. \r\nThe bedrock in the Anchorage area is chiefly Tertiary shale in the lowland \r\nand metamorphic rocks of Mesozoic age beneath the adjacent mountain \r\nslopes. Glacial drift which underlies nearly the entire area has an average \r\nthickness of several hundred feet and appears to include at least five sheets \r\nof deposits, two of which are exposed. The drift consists of till, outwash stream and lake deposits (sand and gravel), and estuarine (and lake) deposits \r\n(clay and silt). The stratigraphy and lateral distribution of the deposits are \r\ncomplex, but data at hand s, how that the thickest deposits, including all the \r\nestuarine and lake sediment and most of the stream-deposited sediment, \r\nare beneath the lowland away from the mountain wall, and that the deposits \r\nnear the mountains are till and subordinate outwash sediments. \r\nDeposits of sand and gravel laid down by outwash streams in channels and \r\non outwash plains are the most important aquifers, and the only \r\nones which yield large quantities of ground water from single beds. Thin \r\nlayers of sandy or gravelly material in till are also important aquifers although they yield relatively small quantities of water. Bedded sand and \r\nsilt associated with the estuarine and lake(?) clay commonly becomes unstable during drilling and pumping, and has been successfully developed in \r\nonly a few wells. Unconfined aquifers are extensive, but permeable saturated \r\nmaterial is thin in many places and water supplies available from them are \r\nsmall or undependable in those places. The most important aquifers are confined or artesian. Clay and till form the confining beds: the till is somewhat 'leaky' in many places. Near Anchorage the buried water-bearing \r\nbeds appear to be interconnected and to form a single artesian system. The \r\nwater table and piezometric surface slope from the mountain wall of the \r\nlowland toward the estuaries, and the flow of the ground water is in that \r\ndirection. The aquifers are recharged by the infiltration of precipitation \r\nat the land surface and of surface water through stream beds: near the mountains the artesian aquifers are probably recharged in part by percolation from \r\nthe water-table aquifer, and far from the mountains the water-table aquifer \r\nis probably recharged in part by upward flow from the underlying artesian \r\naquifers. In several valleys and in a few other places, in the lowland, artesian wells flow at the land surface. \r\nThe outwash sand and gravel are moderately to very permeable; most \r\nof the other water-bearing material are much less permeable. The co- efficient of transmissibility for some single beds of sandy gravel is as high \r\nas 60,000 to I00,000 gpd per ft (gallons per day per foot); for the entire \r\nsection of glacial drift at and near Anchorage it is believed to be of the \r\norder of 200,000 gpd per ft. Calculations based on this value for the total \r\nsection and on the slope of the piezometric surface indicate that in the \r\nimmediate vicinity of Anchorage about 5 million gpd flows through each \r\nmile-wide section of the drift (measured in a northeast-southwest direction, perpendicular to the direction of flow), under normal (nonpumping) conditions. Under conditions of continuous heavy pumping the slope of the piezometric surface is steepened, flow is increased, and additional recharge is induced. \r\n\r\nThe highest yield reported from a well in this area is 2.600 gpm (gallons per minute) with 35 feet of drawdown: the highest reported specific capacity is 180 gpm per ft of drawdown, for a well pumped at. 270 gpm. \r\n\r\nOnly a few wells in the area have been developed for high yields. Well screens have been used ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1773","usgsCitation":"Cederstrom, D.J., Trainer, F.W., and Waller, R.M., 1964, Geology and ground-water resources of the Anchorage area, Alaska: U.S. Geological Survey Water Supply Paper 1773, vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1773.","productDescription":"vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138014,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1773/report-thumb.jpg"},{"id":25887,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25888,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25889,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25890,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25891,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1773/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6855f4","contributors":{"authors":[{"text":"Cederstrom, Dagfin John","contributorId":90287,"corporation":false,"usgs":true,"family":"Cederstrom","given":"Dagfin","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":143212,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trainer, Frank W.","contributorId":103655,"corporation":false,"usgs":true,"family":"Trainer","given":"Frank","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143213,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waller, Roger Milton","contributorId":22320,"corporation":false,"usgs":true,"family":"Waller","given":"Roger","email":"","middleInitial":"Milton","affiliations":[],"preferred":false,"id":143211,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2029,"text":"wsp1617A - 1964 - Discharge characteristics of embankment-shaped weirs","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1617A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1617","chapter":"A","title":"Discharge characteristics of embankment-shaped weirs","docAbstract":"An embankment-shaped weir is an embankment overtopped by flood waters. Among the engineering problems frequently resulting from. this occurrence is the need to compute the peak discharge from postflood yield observations. The research described in this. report was concerned with the theoretical and experimental bases for the computation procedure. \r\n\r\nThe research had two main objectives. One was to determine the relationship between embankment form and roughness and some of the more important discharge characteristics. The second was to define, theoretically and experimentally, the relationship between free-flow discharge and the boundary layer on the roadway. The first objective was accomplished with the experimental determination of coefficients of discharge and other significant flow characteristics for a variety of boundary and flow conditions. The second objective was accomplished with the development and experimental verification of a discharge equation which involved the boundary layer displacement thickness. This phase of the research included a general investigation of boundary layer growth on the roadway. \r\n\r\nIt is included that both free- and submerged-flow discharge are virtually independent of the influence of embankment shape and relative height. The influence of boundary resistance is appreciable only for smaller heads. The most practical solution for discharge is one which is based on. the simple weir equation and experimentally determined coefficients. A completely analytical equation of discharge is impractical. \r\n\r\nThe report contains the results of 936 experiments on the discharge characteristics of 17 different models; plus 106 boundary-layer velocity traverses on 4 different models. The data are summarized in both graphical and tabular form.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1617A","usgsCitation":"Kindsvater, C.E., 1964, Discharge characteristics of embankment-shaped weirs: U.S. Geological Survey Water Supply Paper 1617, v, 11 p. :tables, graphs, diagrs, illus. ;24 cm., https://doi.org/10.3133/wsp1617A.","productDescription":"v, 11 p. :tables, graphs, diagrs, illus. ;24 cm.","costCenters":[],"links":[{"id":137646,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1617a/report-thumb.jpg"},{"id":27502,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1617a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae939","contributors":{"authors":[{"text":"Kindsvater, Carl E.","contributorId":73182,"corporation":false,"usgs":true,"family":"Kindsvater","given":"Carl","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144552,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2186,"text":"wsp1747 - 1964 - Geology and hydrology of the West Milton area, Saratoga County, New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1747","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"1747","title":"Geology and hydrology of the West Milton area, Saratoga County, New York","docAbstract":"This report describes the geology, ground-water conditions, streamflow characteristics, and quality of water in the West Milton area, Saratoga County, N.Y. The West Milton area is in the east-central part of New York in the hilly region that forms a transition zone between the Adirondack Mountains and the Hudson-Mohawk valley lowland. Bedrock underlying the area consists of crystalline rocks of Precambrian age and sandstone, dolomite, limestone, and shale formations of Cambrian and Ordovician age. The formations have been moderately folded and have been displaced as much as several hundred feet' along at least three northeast-trending normal faults. The bedrock is overlain in nearly all parts of the area by a layer of unconsolidated deposits which ranges in thickness from a few feet to more than 200 feet. The unconsolidated deposits are of Pleistocene age and consist of unstratified materials (till) laid down by glacial ice at stratified sediments deposited by glacial meltwaters. The topography of the bedrock surface differs greatly from the topography of the land surface. Although not evident in the present topography, at least two channels, cut in bedrock by preglacial streams, pass through the area. \r\n\r\nGround-water supplies adequate to satisfy domestic requirements can be obtained from wells in any part of the area. Large ground-water supplies may be taken from coarse-grained stratified deposits comprising two aquifers in the valley of Kayaderosseras Creek. The Atomic Energy Commission has pumped as much as 1 mgd from a horizontal well drawing from the uppermost aquifer which is composed of flood-plain deposits. Part of the water yielded by this well during extended periods of pumping is induced flow from the creek. Three nearby vertical wells drilled by the Commission comprise a separate well field capable of yielding at least 2 mgd and possibly as much as 3 mgd from the deeper stratified deposits underlying the valley. A pumping test showed that at near the center of this well field the coefficient of transmissibility is about 125,000 gpd per ft and the coefficient of storage is about 0.0003. The water obtained from the sand and gravel has a hardness of about 125 ppm and contains about 150 ppm of dissolved solids. \r\n\r\nMost of the Government reservation is drained by Glowegee Creek, one of the larger tributaries of Kayaderosseras Creek. The average streamflow of Kayaderosseras Creek at West Milton is 141 cfs or about 1.5 cfs per sq. mi. The monthly mean discharge has ranged from a low of 21.7 cfs in September 1958 to a high of 866 cfs in March 1936, and the annual mean discharge has ranged from 94.5 cfs in 1941 to 198 cfs in 1952. The mean annual flood is 1,740 cfs and the 50-year flood is 5,300 cfs. \r\n\r\nStreamflow data have been collected on Glowegee Creek since 1948 at a station 0.5 mile south of West Milton. The average streamflow of Glowegee Creek at this station is 41 cfs or about 1.5 cfs per sq mi. The mean annual flood is 740 cfs and the 50-year flood is 2,250 cfs. \r\n\r\nThe quality of the water in both Kayaderosseras Creek and Glowegee Creek is satisfactory for public supply and most industrial purposes. The mineral content of both streams is low--the dissolved-solids content averaging about 93 ppm in Kayaderosseras Creek and about 131 ppm in Glowegee Creek. The average hardness of water in Kayaderosseras Creek and Glowegee Creek is 68 ppm and 102 ppm, respectively. During periods of low flow, suspended sediment discharge in both streams is less than 10 tons per day, but during periods of high flow, the sediment discharge has been as great as 163 tons per day in Glowegee Creek and 437 tons per day in Kayaderosseras Creek.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1747","usgsCitation":"Mack, F., Pauszek, F.H., and Crippen, J.R., 1964, Geology and hydrology of the West Milton area, Saratoga County, New York: U.S. Geological Survey Water Supply Paper 1747, viii, 110 p. :illus., maps, diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1747.","productDescription":"viii, 110 p. :illus., maps, diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":137741,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1747/report-thumb.jpg"},{"id":27816,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27817,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27818,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27819,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27820,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27821,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1747/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27815,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b4691","contributors":{"authors":[{"text":"Mack, Frederick K.","contributorId":95858,"corporation":false,"usgs":true,"family":"Mack","given":"Frederick K.","affiliations":[],"preferred":false,"id":144794,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pauszek, F. H.","contributorId":61399,"corporation":false,"usgs":true,"family":"Pauszek","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144793,"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":144792,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70221132,"text":"70221132 - 1964 - Hydrologic factors pertinent to ground‐water contamination","interactions":[],"lastModifiedDate":"2021-06-04T12:04:08.414151","indexId":"70221132","displayToPublicDate":"1964-01-01T13:47:53","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Hydrologic factors pertinent to ground‐water contamination","docAbstract":"Predictions of where and how a fluid waste may travel from disposal site to the water table require detailed information on the physical characteristics, location, and extent of all pervious and impervious materials in the unsaturated zone. Principles concerning the flow system in the unsaturated zone indicate the importance of choice of disposal technique in predicting the time required for the fluid waste to traverse the distance to the water table. With appropriate data on the location, extent, and physical properties of water‐bearing materials and on the boundaries of the saturated zone flow system, it is possible to analyze the relative merits of a variety of waste disposal techniques and to describe the probable consequences of each. Environments of consolidated rocks, such as granites, sandstones, and limestones, pose problems in addition to those related to unconsolidated or granular porous media in defining the fluid‐flow regimes that involve joint patterns, fracture patterns, solutional openings, and the rock structure. The consequences of ground‐water contamination can be just as damaging to water users as the pollution of surface streams. In fact it can be argued that the consequences are far more damaging because they persist over much longer periods of time after the contaminating source has been eliminated. It would appear prudent, therefore, to guard against contamination of the ground‐water resource in the first instance, rather than to engage in long expensive rehabilitation measures after the damage has been done. In 1960 Graham Walton presented data concerning contamination, by sewage or other man‐made wastes, of surface and underground waters. The circumstances attending the reported incidents of contamination, especially those involving ground‐water supplies, have aided materially in the choice of a few principles and ideas that will identify the role of some significant hydrologic factors in the underground movement of fluid wastes. Walton's discussion of ground‐water contamination refers often to physical settings into which fluid wastes are discharged at or near the land surface into cesspools, tile‐drain fields, and holding ponds. Furthermore, most reported instances of ground‐water contamination have taken place in relatively humid.
","language":"English","publisher":"NGWA The Groundwater Association","doi":"10.1111/j.1745-6584.1964.tb01739.x","usgsCitation":"Brown, R., 1964, Hydrologic factors pertinent to ground‐water contamination: Groundwater, v. 2, no. 1, p. 5-12, https://doi.org/10.1111/j.1745-6584.1964.tb01739.x.","productDescription":"8 p.","startPage":"5","endPage":"12","costCenters":[],"links":[{"id":386191,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"2","issue":"1","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Brown, R.","contributorId":101419,"corporation":false,"usgs":true,"family":"Brown","given":"R.","affiliations":[],"preferred":false,"id":816940,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221133,"text":"70221133 - 1964 - Hydrologic factors pertinent to ground‐water contamination","interactions":[],"lastModifiedDate":"2021-06-02T18:50:54.556763","indexId":"70221133","displayToPublicDate":"1964-01-01T13:47:53","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Hydrologic factors pertinent to ground‐water contamination","docAbstract":"Predictions of where and how a fluid waste may travel from disposal site to the water table require detailed information on the physical characteristics, location, and extent of all pervious and impervious materials in the unsaturated zone. Principles concerning the flow system in the unsaturated zone indicate the importance of choice of disposal technique in predicting the time required for the fluid waste to traverse the distance to the water table. With appropriate data on the location, extent, and physical properties of water‐bearing materials and on the boundaries of the saturated zone flow system, it is possible to analyze the relative merits of a variety of waste disposal techniques and to describe the probable consequences of each. Environments of consolidated rocks, such as granites, sandstones, and limestones, pose problems in addition to those related to unconsolidated or granular porous media in defining the fluid‐flow regimes that involve joint patterns, fracture patterns, solutional openings, and the rock structure. The consequences of ground‐water contamination can be just as damaging to water users as the pollution of surface streams. In fact it can be argued that the consequences are far more damaging because they persist over much longer periods of time after the contaminating source has been eliminated. It would appear prudent, therefore, to guard against contamination of the ground‐water resource in the first instance, rather than to engage in long expensive rehabilitation measures after the damage has been done. In 1960 Graham Walton presented data concerning contamination, by sewage or other man‐made wastes, of surface and underground waters. The circumstances attending the reported incidents of contamination, especially those involving ground‐water supplies, have aided materially in the choice of a few principles and ideas that will identify the role of some significant hydrologic factors in the underground movement of fluid wastes. Walton's discussion of ground‐water contamination refers often to physical settings into which fluid wastes are discharged at or near the land surface into cesspools, tile‐drain fields, and holding ponds. Furthermore, most reported instances of ground‐water contamination have taken place in relatively humid.
","language":"English","publisher":"Wiley Blackwell","doi":"10.1111/j.1745-6584.1964.tb01739.x","usgsCitation":"Brown, R., 1964, Hydrologic factors pertinent to ground‐water contamination: Groundwater, v. 2, no. 1, p. 5-12, https://doi.org/10.1111/j.1745-6584.1964.tb01739.x.","productDescription":"8 p.","startPage":"5","endPage":"12","costCenters":[],"links":[{"id":386147,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"2","issue":"1","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Brown, R.","contributorId":101419,"corporation":false,"usgs":true,"family":"Brown","given":"R.","affiliations":[],"preferred":false,"id":816821,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":35360,"text":"b1133C - 1963 - Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site","interactions":[],"lastModifiedDate":"2018-03-19T10:38:39","indexId":"b1133C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1133","chapter":"C","title":"Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site","docAbstract":"The Elk River, Minn., nuclear-reactor site is on the east bluff of the Mississippi River about 35 miles northwest of Minneapolis and St. Paul. The area is underlain by about 70 to 180 feet of glacial drift, including at the top as much as 120 feet of outwash deposits (valley train) of the glacial Mississippi River. The underlying Cambrian bedrock consists of marine sedimentary formations including artesian sandstone aquifers. A hypothetically spilled liquid at the reactor site could follow one or both of two courses, thus: (1) It could flow over the land surface and through an artificial drainage system to the river in a matter of minutes; (2) part or nearly all of it could seep downward to the water table and then move laterally to the river. The time required might range from a few weeks to a year, or perhaps more. The St. Paul and Minneapolis water-supply intakes, 21 and 25 miles downstream, respectively, are the most critical points to be considered in the event of an accidental spill. Based on streamflow and velocity data for the Mississippi River near Anoka, the time required for the maximum concentration of a contaminant to travel from the reactor site to the St. Paul intake was computed to be about 8 hours, at the median annual maximum daily discharge. For this discharge, the maximum concentration at the intake would be about 0.0026 microcurie per cubic foot for the release of 1 curie of activity into the river near the reactor site.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/b1133C","collaboration":"Prepared in cooperation with the U.S. Atomic Energy Commission","usgsCitation":"Norvitch, R.F., Schneider, R., and Godfrey, R.G., 1963, Geology and hydrology of the Elk River, Minnesota, nuclear-reactor site: U.S. Geological Survey Bulletin 1133, Document: iv, 25 p.; 2 Plates: 18 x 16 inches, https://doi.org/10.3133/b1133C.","productDescription":"Document: iv, 25 p.; 2 Plates: 18 x 16 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":63222,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1133c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63223,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1133c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63224,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1133c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109385,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20849.htm","linkFileType":{"id":5,"text":"html"},"description":"20849"},{"id":165594,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1133c/report-thumb.jpg"}],"country":"United States","state":"Minnesota","city":"Elk River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.61209869384766,\n 45.261596972270866\n ],\n [\n -93.61209869384766,\n 45.3297027614069\n ],\n [\n -93.51133346557617,\n 45.3297027614069\n ],\n [\n -93.51133346557617,\n 45.261596972270866\n ],\n [\n -93.61209869384766,\n 45.261596972270866\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b468c","contributors":{"authors":[{"text":"Norvitch, Ralph F.","contributorId":65456,"corporation":false,"usgs":true,"family":"Norvitch","given":"Ralph","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":214511,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":214513,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Godfrey, Richard G.","contributorId":100046,"corporation":false,"usgs":true,"family":"Godfrey","given":"Richard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":214512,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":6219,"text":"pp422B - 1963 - Hydraulic geometry of a small tidal estuary","interactions":[],"lastModifiedDate":"2017-03-24T16:16:21","indexId":"pp422B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"422","chapter":"B","title":"Hydraulic geometry of a small tidal estuary","docAbstract":"A tidal channel in a marsh bordering the Potomac River near Alexandria, Va., was mapped, and current-meter measurements of discharge were made at various locations and at various stages in the tidal cycle. These measurements allowed analysis of the change of width, depth, and velocity with discharge at various cross sections and along the length of the channel.
There is also presented a theoretical development of some, of these same relations based on hydraulic principles and on the assumption of a uniform distribution of energy and a minimum rate of work in the system as a whole.
The change of width, depth, and velocity with discharge downstream developed from the field data checked closely with the theoretically derived values.
The estuarine channel differs from a terrestrial one in that discharge at any section in an estuary varies depending on how the flow shaped the entire length of the channel between the point in question and the main body of tidal water. The result is that a tidal channel changes more rapidly in width and less rapidly in depth as discharge changes downstream than does a terrestrial channel.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp422B","usgsCitation":"Myrick, R.M., and Leopold, L.B., 1963, Hydraulic geometry of a small tidal estuary: U.S. Geological Survey Professional Paper 422, 19 p., https://doi.org/10.3133/pp422B.","productDescription":"19 p.","startPage":"B1","endPage":"B18","numberOfPages":"22","costCenters":[],"links":[{"id":140192,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0422b/report-thumb.jpg"},{"id":94745,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0422b/report.pdf","size":"2291","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Virginia","city":"Alexandria, VA","otherGeospatial":"Potomac River, Wrecked Recorded Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.05480098724365,\n 38.7592035579107\n ],\n [\n -77.04287052154541,\n 38.7592035579107\n ],\n [\n -77.04287052154541,\n 38.77817551784403\n ],\n [\n -77.05480098724365,\n 38.77817551784403\n ],\n [\n -77.05480098724365,\n 38.7592035579107\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62a200","contributors":{"authors":[{"text":"Myrick, Robert M.","contributorId":24345,"corporation":false,"usgs":true,"family":"Myrick","given":"Robert","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":152320,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":152321,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":14201,"text":"ofr5956 - 1963 - Geology of the Anlauf and Drain quadrangles, Douglas and Lane counties, Oregon","interactions":[{"subject":{"id":14201,"text":"ofr5956 - 1963 - Geology of the Anlauf and Drain quadrangles, Douglas and Lane counties, Oregon","indexId":"ofr5956","publicationYear":"1963","noYear":false,"title":"Geology of the Anlauf and Drain quadrangles, Douglas and Lane counties, Oregon"},"predicate":"SUPERSEDED_BY","object":{"id":34704,"text":"b1122D - 1963 - Geology of the Anlauf and Drain Quadrangles, Douglas and Lane Counties, Oregon","indexId":"b1122D","publicationYear":"1963","noYear":false,"chapter":"D","title":"Geology of the Anlauf and Drain Quadrangles, Douglas and Lane Counties, Oregon"},"id":1}],"supersededBy":{"id":34704,"text":"b1122D - 1963 - Geology of the Anlauf and Drain Quadrangles, Douglas and Lane Counties, Oregon","indexId":"b1122D","publicationYear":"1963","noYear":false,"title":"Geology of the Anlauf and Drain Quadrangles, Douglas and Lane Counties, Oregon"},"lastModifiedDate":"2024-07-15T18:35:49.634771","indexId":"ofr5956","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"59-56","title":"Geology of the Anlauf and Drain quadrangles, Douglas and Lane counties, Oregon","docAbstract":"The Anlauf and Drain quadrangles, Oregon, lie about 20 miles south of the City of Eugene, in Douglas and Lane Counties. They constitute an area of about 435 square miles that includes parts of both the Cascade Range and Coast Range physiographic provinces.
A sequence of lower Tertiary sedimentary and volcanic rocks with a maximum thickness of about 20,000 feet is exposed in the area. The oldest part of this sequence is the Umpqua formation of early Eocene age consisting of a lower Member of vesicular and amygdaloidal olivine basalt flows, a middle member of water-laid vitric and lapilli crystal tuff, and an upper member of interbedded fissile siltstone and basaltic sandstone which contains a 300-foot tongue of massive to thick-bedded basaltic sandstone near its top. These rocks are predominantly of marine origin, although the general absence of pillow structures Which are common in basaltic lavas of equivalent age elsewhere in the Coast Ranges suggests that some of the flows were poured out subaerially. The overlying tuff member, however, contains Foraminifera and in places has a lime content slightly in excess of 10 percent. Mollusca and Foraminifera indicate that the Umpqua formation is of early Eocene age and is a correlative of the Capay formation of California.
The Tyee formation of middle Eocene age overlies the Umpqua formation and consists of more than 5,000 feet of rhythmically deposited sandstone and siltstone in beds 2 to 30 feet thick. The basal part of each bed consists of medium- to coarse-grained sandstone that grades upward into line-grained sandstone and siltstone. The principal constituents of the sandstone are quartz, partly altered feldspar, mica, clay, and fragments of basalt, fine-grained argillaceous rocks, and mica schist. Other detrital minerals include epidote, garnet, blue-green hornblende, tourmaline, and zoisite. The depositional environment of the Tyee formation is poorly known, although the rhythmic-graded bedding suggests turbidity currents.
About 500 feet of sandstone and siltstone assigned to the Spencer formation of late Eocene age unconformably overlies the Tyee formation. The Spencer formation, better exposed in the east-central part of the Coast Ranges, contains marine fossils but also has thin impure coal beds, indicative of strand-line accumulation. The sandstone in the Spencer formation is very similar to that in the Tyee formation, from which it was probably derived.
The Fisher formation contains about 5,500 feet of nonmarine pyroclastic and Volcanic rocks that are related to the volcanic rock sequences of the western Cascade Range. The formation is characterized by a wide variety of rock types, including conglomerate, tuffaceous sandstone and siltstone, vitric and crystal tuff, waterlaid and mudflow breccia, and andesitic lava flows. These rocks generally occur in lenticular beds that have little stratigraphic significance. The rocks apparently accumulated on a plain slightly above sea level that was subjected alternately to flooding by running water and to desiccation. Fossil leaves from the lowermost part of the Fisher formation are of late Eocene age; the upper part of the formation is of early, and possibly middle, Oligocene age.
A few exposures of olivine basalt were mapped in the extreme northern part of the Anlauf quadrangle. The flows, more extensively exposed to the north, overlie the Fisher formation, and, therefore, are tentatively considered to be post-Oligocene in age.
All these stratigraphic units, but principally the Fisher formation, are cut by dikes, sills, and stocklike bodies of porphyritic basalt, diabase, and norite. Contemporaneously with the emplacement of most of these rocks, in late Miocene(?) time, hydrothermal solutions locally altered the sedimentary and extrusive igneous rocks and deposited cinnabar and other sulfide minerals, carbonates, and silica.
Three parallel northeastward-trending anticlines in the older marine rocks are the most conspicuous structural features in the area. These folds plunge both to the northeast and southwest and expose in their central parts basalt flows of the Umpqua formation. The rocks along the west margin of the area dip westward into a structural basin in the adjacent Elkton quadrangle, whereas to the east the Fisher formation generally has an easterly dip typical of the nonmarine rocks in the western Cascade Range.
Geologic studies in the Anlauf and Drain quadrangles were undertaken principally to evaluate the petroleum possibilities of the area. Available data indicate that source beds and reservoir rock suitable for the formation and accumulation of petroleum are absent in this part of the Coast Ranges, but because of the lack of subsurface information, this evaluation is only tentative. Mineral deposits of economic value in the area include quicksilver and alumina clay.
The magnitude of a flood of any selected frequency up to 50 years for any site on any stream in the Snake River basin can be determined by methods outlined in this report, with some limitations. The methods are not applicable for regulated streams, for drainage basins smaller than 10 or larger than 5,000 square miles, for streams fed by large springs, or for streams that have flow characteristics materially different from the regional pattern. The magnitude of a flood for a selected frequency at a given site is determined by using the appropriate composite frequency curve and the mean annual flood for the given site. The mean annual flood is computed from either a formula or a nomograph in which drainage area, mean annual precipitation, and a geographic factor are used as independent variables. The standard error of estimate for the computation of mean annual floods is plus 17 percent and minus 15 percent.
Nine flood-frequency regions (A-I) are defined. In all except regions B and I, frequency relations vary with the mean altitude of the basin as well as with the geographic location; therefore, families of curves are required for 7 of the 9 flood-frequency regions.
The report includes a brief description of the physiography and climate of the Snake River basin to explain the reason for the large variation in mean annual floods, which range from zero to about 27 cubic feet per second per square mile.
Composite frequency curves and formulas for computing mean annual floods are based on all suitable flood data collected in the Snake River basin. Tables show the data used to derive the formula. Following the analysis of data are station descriptions and lists of peak stages and discharges for 295 gaging stations at which 5 or more years of annual flood records were collected pr'or to Sept. 30, 1957. Many flood peak data are not usable in defining the frequency curves and deriving the formula because of large diversions and regulation upstream from the gaging stations.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1688","usgsCitation":"Thomas, C., Broom, H.C., and Cummans, J., 1963, Magnitude and frequency of floods in the United States, part 13. Snake River basin: U.S. Geological Survey Water Supply Paper 1688, Report: xi, 250 p.; 5 Plates: 31.50 x 31.36 inches or smaller, https://doi.org/10.3133/wsp1688.","productDescription":"Report: xi, 250 p.; 5 Plates: 31.50 x 31.36 inches or smaller","numberOfPages":"266","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":395475,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24897.htm"},{"id":29339,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1688/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29338,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1688/plate-5.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Snake River basin showing geographic factors"},{"id":29337,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1688/plate-4.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Snake River basin showing flood regions"},{"id":29336,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1688/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of Snake River basin showing location of gaging stations with 5 or more years of annual flood record"},{"id":29335,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1688/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Precipitation index map of the Snake River basin"},{"id":29334,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1688/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of physiographic regions of Snake River basin"},{"id":138808,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1688/report-thumb.jpg"}],"country":"United States","state":"Idaho, Nevada, Oregon, Utah, Washington, Wyoming","otherGeospatial":"Snake River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119,\n 41.167\n ],\n [\n -110,\n 41.167\n ],\n [\n -110,\n 47.333\n ],\n [\n -119,\n 47.333\n ],\n [\n -119,\n 41.167\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649611","contributors":{"authors":[{"text":"Thomas, C.A.","contributorId":14385,"corporation":false,"usgs":true,"family":"Thomas","given":"C.A.","email":"","affiliations":[],"preferred":false,"id":145835,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Broom, H. C.","contributorId":93024,"corporation":false,"usgs":true,"family":"Broom","given":"H.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":145837,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cummans, J. E.","contributorId":24767,"corporation":false,"usgs":true,"family":"Cummans","given":"J. E.","affiliations":[],"preferred":false,"id":145836,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":57727,"text":"ofr63151 - 1963 - Surface water of Little River basin in southeastern Oklahoma (with a section on quality of water by R. P. Orth)","interactions":[],"lastModifiedDate":"2012-02-02T00:12:12","indexId":"ofr63151","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-151","title":"Surface water of Little River basin in southeastern Oklahoma (with a section on quality of water by R. P. Orth)","docAbstract":"This report summarizes basic hydrologic data of the surface water resources of Little River basin above the Oklahoma-Arkansas state line near Cerrogordo, Okla., and by analysis and interpretation, presents certain streamflow characteristics at specified points in the basin.\r\nLittle River basin above the state line includes 2,269 square miles, of which about 250 square miles of the Mountain Fork River is in Arkansas. The climate is humid and the annual precipitation averages about 46 inches. Gross annual lake evaporation averages 49 inches per year. There are three reservoirs totaling 2,831,800 acre-feet of storage, either authorized or under construction in the basin.\r\n\r\nThe average annual discharge at the gaging stations for the period 1930-61 is 674,900 acre-feet for Little River near Wright City; 1,273,000 acre-feet for Little River below Lukfata Creek, near Idabel; and 989,000 acre-feet for Mountain Fork River near Eagletown. The average annual discharge of Little River at the Oklahoma-Arkansas state line near Cerrogordo is 2,401,000 acre-feet.\r\n\r\nFlow-duration curves have been developed from daily records for the gaging stations. These curves show the percentage of time various rates of discharge have been equaled or exceeded. Procedures for defining the frequency of annual floods at any point in the basin are given. Low-flow frequency curves for the gaging stations defining the recurrence intervals of 7, 14 or 15, 30, 60, and 120 day mean flows have been prepared. Curves showing the relation of instantaneous discharge at specified upstream points to the daily mean discharge at two gaging stations are presented. The storage requirements for suplementing natural flows have been prepared for the gaging-station sites. Chemical analyses show that the surface water in the basin is suitable for domestic and industrial uses.","language":"ENGLISH","doi":"10.3133/ofr63151","usgsCitation":"Westfall, A., and Orth, R.P., 1963, Surface water of Little River basin in southeastern Oklahoma (with a section on quality of water by R. P. Orth): U.S. Geological Survey Open-File Report 63-151, 66 leaves : ill., map ; 29 cm., https://doi.org/10.3133/ofr63151.","productDescription":"66 leaves : ill., map ; 29 cm.","costCenters":[],"links":[{"id":184344,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db697eda","contributors":{"authors":[{"text":"Westfall, A.O.","contributorId":85225,"corporation":false,"usgs":true,"family":"Westfall","given":"A.O.","email":"","affiliations":[],"preferred":false,"id":257649,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Orth, Richard Philip","contributorId":56725,"corporation":false,"usgs":true,"family":"Orth","given":"Richard","email":"","middleInitial":"Philip","affiliations":[],"preferred":false,"id":257648,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":57726,"text":"ofr63150 - 1963 - Ground-water levels in observation wells in Oklahoma, 1956-1960","interactions":[],"lastModifiedDate":"2018-11-08T15:38:34","indexId":"ofr63150","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-150","title":"Ground-water levels in observation wells in Oklahoma, 1956-1960","docAbstract":"The investigation of the ground-water resources of Oklahoma by the U.S. Geological Survey in cooperation with the Oklahoma Water Resources Board includes a continuing program to collect on a systematic basis records of water levels in selected observation wells. These water-level records: (1) provide an index to available ground-water supplies; (2) facilitate the prediction of trends in water levels that will indicate likely changes in storage; (3) aid in the prediction of the base flow of streams; (4) provide information for use in basic research; and (5) provide long-time continuous records of fluctuations of water levels in representative wells, These selected records also serve as a framework to which other types of hydrologic data may be related.
Prior to 1956, measurements of water levels in observation wells in Oklahoma were included in water-supply papers published annually by the U.S. Geological Survey (table 1). Beginning with the 1956 calendar year, however, Federal water-level reports will contain only records of a selected network of observation wells, and will be published by the U.S. Geological Survey at 5-year intervals. The first of this series, for the 1956-59 period has recently been published.
This report has been prepared primarily to present water-level records of wells not included in the Federal network. However, for the sake of completeness it includes water-level records of Federal wells that either have been or will be published in Water-Supply Papers since 1955. This report, which contains water-level records for the 5-year period (1956-60), is the first of a series presenting water-level records for all permanent observation wells in Oklahoma. It is planned that future water-level reports will be published at 2-year intervals.
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Jr.","contributorId":49403,"corporation":false,"usgs":true,"family":"Hart","given":"D.L.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":257647,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":57725,"text":"ofr63148 - 1963 - Surface water of Muddy Boggy River basin in south-central Oklahoma","interactions":[],"lastModifiedDate":"2012-02-02T00:12:12","indexId":"ofr63148","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-148","title":"Surface water of Muddy Boggy River basin in south-central Oklahoma","docAbstract":"This report summarizes basic hydrologic data of the surface water resources of Muddy Boggy River basin, and by analysis and interpretation, presents certain streamflow characteristics at specified points in the basin.\r\nMuddy Boggy River has a drainage area of 2,429 square miles. The climate is moist subhumid and the annual precipitation averages about 39 inches. Gross annual lake evaporation averages 54 inches.\r\n\r\nThe average annual discharge at the gaging stations for the period 1938-62 was 24,000 acre-feet for Chickasaw Creek near Stringtown; 72,000 acre-feet for McGee Creek near Stringtown; 671,800 acre-feet for Muddy Boggy Creek near Farris; and 358,200 acre-feet for Clear Boggy Creek near Caney.\r\n\r\nFlow-duration curves of daily discharge have been developed to show the percentage of time various rates of discharge have been equaled or exceeded. Procedures for determining the frequency of annual floods at any point in the basin are given. Low-flow frequency curves that define the recurrence intervals of 7, 14, 30, 60, and 120 day mean flows have been prepared for two gaging stations. Curves showing the relation of measured discharge at the low-flow partial-record stations to the daily mean discharge at a base gaging station are presented. Discharge measurements made in February 1963 at selected sites show the areal distribution of low flow. The storage requirements to supplement natural flows have been prepared for two gaging-stations sites.\r\n\r\nThe chemical quality of surface water of Muddy Boggy River basin varies from place-to-place during base flow periods. Limestone and dolomite outcrops and oilfield brines affect water quality in some areas. Water of North Boggy Creek, McGee Creek, and their tributaries contains less than 100 ppm (parts per million) dissolved solids. Water of other streams in Muddy Boggy River basin has a higher dissolved-solids content, but the content does not exceed 500 ppm. Water of Muddy Boggy River basin is usable for domestic, irrigation, and most industrial purposes. Softening of water from some streams may be desirable, however.","language":"ENGLISH","doi":"10.3133/ofr63148","usgsCitation":"Westfall, A., and Cummings, T.R., 1963, Surface water of Muddy Boggy River basin in south-central Oklahoma: U.S. Geological Survey Open-File Report 63-148, 71 p. : ill., map ; 29 cm., https://doi.org/10.3133/ofr63148.","productDescription":"71 p. : ill., map ; 29 cm.","costCenters":[],"links":[{"id":184342,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afbe4b07f02db6962be","contributors":{"authors":[{"text":"Westfall, A.O.","contributorId":85225,"corporation":false,"usgs":true,"family":"Westfall","given":"A.O.","email":"","affiliations":[],"preferred":false,"id":257646,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cummings, T. Ray","contributorId":20722,"corporation":false,"usgs":true,"family":"Cummings","given":"T.","email":"","middleInitial":"Ray","affiliations":[],"preferred":false,"id":257645,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2382,"text":"wsp1614 - 1963 - Water resources of Red River Parish, Louisiana","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1614","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1614","title":"Water resources of Red River Parish, Louisiana","docAbstract":"Red River Parish is on the eastern flank of the Sabine uplift in northwestern Louisiana. The 'area is underlain by lignitic clay and sand of Paleocene and Eocene age which dip to the east at the rate of about 30 feet per mile. The Red River is entrenched in these rocks in the western part of the parish. Alternating valley filling and erosion during the Quaternary period have resulted in the present lowland with flanking terraces. \r\n\r\nIn the flood-plain area moderate to large quantities of very hard, iron-bearing water, suitable for irrigation, are available to wells in the alluvial sand and gravel of Quaternary age. The aquifer ranges in thickness from 20 to slightly more than 100 feet. It is recharged by downward seepage of rainfall through overlying clay and silt, by inflow from older sands adjacent to and beneath the entrenched valley, and by infiltration from the streams where the water table is below stream level during flood stages or as a result of pumping. Water levels are highest in the middle of the valley. Ground water moves mainly toward the Red River on the east and Bayou Pierre on the west, but small amounts move down the valley. Computations based on water-level and aquifer-test data indicate that the Quaternary alluvium contains more than 330 billion gallons of ground water in storage and that the maximum discharge of ground water to the streams is slightly more than 30 mgd (million gallons per day). At times of high river stage, surface water flows into the aquifer at a rate that depends in part upon the height and duration of the river stage. \r\n\r\nModerate supplies of soft, iron-bearing water may be obtained from dissected Pleistocene terrace deposits that flank the flood plains of the Red River and Black Lake Bayou. However, the quantity of water that can be pumped from these deposits varies widely from place to place because of differences in the areal extent and saturated thickness of the segments of the deposits; this extent and thickness are governed in turn by the amount of erosion the deposits have undergone. Beds of fine-grained lignitic sands of Tertiary age contain water of generally good quality to depths of 150 to 450 feet. The thinness and low permeability of the sands restrict their development to low-yield wells. Water from these sands in the western part of the parish, where they lie beneath the alluvial valley, is more mineralized than that from the younger Tertiary sands exposed in the east-central area. \r\n\r\nStreamflow records have been collected on the principal streams in Red River Parish since 1939. Additional spot low-flow data were obtained on several small streams originating within the parish for a study made in connection with the preparation of this report. Quality-of-water data for streams in the parish were collected on an occasional spot-sampling basis prior to and during this investigation. The largest source of surface water in the parish is the Red River, which drains approximately 63,400 square miles upstream from the parish. The Red River has an average flow of about 13,100 cfs (cubic feet per second), or about 8,500 mgd. Many of the streams that drain the upland area are not dependable sources of supply because their flows are not well sustained during dry seasons.\r\n\r\nThe average annual precipitation over the parish is about 52 inches, of which about 17 inches becomes runoff; this runoff is equivalent to a continuous flow of about 1.25 cfs per square mile. Seasonal and annual runoff varies, but no significant trends have been noticed.\r\n\r\nThe principal surface-water problems in the parish pertain to flood control, drainage, irrigation, and navigation. Flood problems have been alleviated considerably by the operation of Denison Dam (Lake Texoma), the completion of levees on the Red River, channel improvements on Bayou Pierre, and the completion of Wallace Lake reservoir on Cypress Bayou. There are wet lands along the Red River that would be very productive if properly drained ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1614","usgsCitation":"Newcome, R., and Page, L.V., 1963, Water resources of Red River Parish, Louisiana: U.S. Geological Survey Water Supply Paper 1614, v, 133 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1614.","productDescription":"v, 133 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":109996,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24808.htm","linkFileType":{"id":5,"text":"html"},"description":"24808"},{"id":137824,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1614/report-thumb.jpg"},{"id":28344,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28345,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28346,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28347,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28348,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28349,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28350,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28351,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28352,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28353,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28354,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28355,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28356,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1614/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28357,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1614/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a16e4b07f02db603d22","contributors":{"authors":[{"text":"Newcome, Roy","contributorId":14796,"corporation":false,"usgs":true,"family":"Newcome","given":"Roy","affiliations":[],"preferred":false,"id":145113,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Page, Leland Vernon","contributorId":95450,"corporation":false,"usgs":true,"family":"Page","given":"Leland","email":"","middleInitial":"Vernon","affiliations":[],"preferred":false,"id":145114,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2180,"text":"wsp1532B - 1963 - Hydrologic and biotic characteristics of grazed and ungrazed watersheds of the Badger Wash basin in western Colorado, 1953-58","interactions":[],"lastModifiedDate":"2022-02-18T22:58:29.389041","indexId":"wsp1532B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1532","chapter":"B","title":"Hydrologic and biotic characteristics of grazed and ungrazed watersheds of the Badger Wash basin in western Colorado, 1953-58","docAbstract":"A comprehensive study of the hydrologic and biotic characteristics of small drainage basins on the Colorado Plateau and the effect of grazing on these characteristics vas begun in 1953. This report presents data obtained during the first 5 years of the proposed 20-year study. \r\n\r\nPeriodic observations were made at permanent transects in 8 paired fenced and unfenced watersheds to characterize plant and ground cover, determine degree of use by livestock and measure changes in watershed cover. Results after 5 years of study indicate that changes in watershed cover have been relatively small on both grazed and ungrazed areas. Changes that did take place were mainly on shale and mixed type .soil. Ground-cover index on mixed type soil was significantly higher, 4 percent, on ungrazed ,areas than on grazed areas at the end of 5 years. \r\n\r\nPlot records were obtained using the Rocky Mountain Infiltrameter at 12 plots in each of the 8 study watersheds to determine the effect of livestock exclusion on infiltration and sheet erosion. Infiltration rates for the last 20 minutes of both the wet .and dry runs were significantly higher in 1958 than they were 5 years before, but this difference was not associated with treatment because rates on both grazed and ungrazed plots increased about .the same amount. The initial water-absorbing capacity increased significantly on ungrazed plots. No change in erosion rates was observed. \r\n\r\nRainfall was variable and below normal during 4 of the first 5 years of study. Runoff was produced mainly by thunderstorms during the summer months and was characterized by high rates of flow for short periods. Comparison of runoff in grazed and ungrazed watersheds indicates a change in the relation between precipitation and runoff because of exclusion of livestock. More sediment per unit area was produced during the 5 years of study from grazed .areas than from ungrazed areas. \r\n\r\nNo definite trend in small mammal population on grazed and ungrazed water- sheds has yet been determined. Results of preliminary studies on rabbit population indicates that rabbits prefer to inhabit ungrazed areas, but populations were judged to be not high in any area.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Hydrologic effects of land use","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U. S. Govt. Print. Off.","doi":"10.3133/wsp1532B","usgsCitation":"Lusby, G.C., Lusby, G.C., Turner, G.T., Thompson, J.R., and Reid, V.H., 1963, Hydrologic and biotic characteristics of grazed and ungrazed watersheds of the Badger Wash basin in western Colorado, 1953-58: U.S. Geological Survey Water Supply Paper 1532, Report: v, 73 p.; 1 Plate: 11.75 × 18.50 inches, https://doi.org/10.3133/wsp1532B.","productDescription":"Report: v, 73 p.; 1 Plate: 11.75 × 18.50 inches","costCenters":[],"links":[{"id":27802,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1532b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27801,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1532b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109967,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24707.htm","linkFileType":{"id":5,"text":"html"},"description":"24707"},{"id":138221,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1532b/report-thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Badger Wash basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.948,\n 39.292\n ],\n [\n -108.91,\n 39.292\n ],\n [\n -108.91,\n 39.356\n ],\n [\n -108.948,\n 39.356\n ],\n [\n -108.948,\n 39.292\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a29e4b07f02db6118ab","contributors":{"authors":[{"text":"Lusby, Gregg C.","contributorId":68290,"corporation":false,"usgs":true,"family":"Lusby","given":"Gregg","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144783,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lusby, George C.","contributorId":102860,"corporation":false,"usgs":true,"family":"Lusby","given":"George","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144784,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Turner, George T.","contributorId":6833,"corporation":false,"usgs":true,"family":"Turner","given":"George","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":144780,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Thompson, J. R.","contributorId":27845,"corporation":false,"usgs":true,"family":"Thompson","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144781,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Reid, Vincent H.","contributorId":57439,"corporation":false,"usgs":true,"family":"Reid","given":"Vincent","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144782,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":14724,"text":"ofr6386 - 1963 - Large uraniferous springs and associated uranium minerals, Shirley Mountains, Carbon County, Wyoming -- A preliminary report","interactions":[],"lastModifiedDate":"2012-02-02T00:06:58","indexId":"ofr6386","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"63-86","title":"Large uraniferous springs and associated uranium minerals, Shirley Mountains, Carbon County, Wyoming -- A preliminary report","docAbstract":"Ten springs along the southeast flank of the Shirley Mountains, Carbon County, Wyoming, have water containing from 12 to 27 parts per billion uranium, have a total estimated flow of 3 million gallons of clear fresh water per day, and have a combined annual output that may be as much as 166 pounds of uranium. These springs emerge from Pennsylvanian, Permian, and Triassic rocks on the east flank of a faulted anticlinal fold. \r\n\r\nIn the vicinity of several springs, metatyuyamunite occurs locally in crystalline calcite veins averaging 3 feet in width but reaching a maximum of 24 feet. The veins are as much as several hundred feet long-and cut vertically through sandstones of Pennsylvanian age overlying the Madison Limestone (Mississippian). This limestone is believed to be the source of the calcite. A 3-foot channel sample cross one calcite vein contains 0.089 percent uranium. Lesser amounts of uranium were obtained from other channel samples. Selected samples contain from 0.39 to 2.2 percent uranium and from 0.25 to 0.86 percent vanadium. \r\n\r\nThree possible sources of the uranium are: (1) Precambrian rocks, (2) Paleozoic rocks, (3) Pliocene(?) tuffaceous strata that were deposited unconformably across older .rocks in both the graphically high and low parts of the area, but were subsequently removed by erosion except for a few small remnants, one of which contains carnotite. \r\n\r\nThere is apparently a close genetic relation between the uraniferous springs and uranium mineralization in the calcite veins. Data from this locality illustrate how uraniferous ground water can be used as a guide in the exploration for areas where uranium deposits may occur. Also demonstrated is the fact that significant quantities of uranium are present in water of some large flowing springs.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6386","usgsCitation":"Love, J.D., 1963, Large uraniferous springs and associated uranium minerals, Shirley Mountains, Carbon County, Wyoming -- A preliminary report: U.S. Geological Survey Open-File Report 63-86, 23 p. ill., folded map ;29 cm., https://doi.org/10.3133/ofr6386.","productDescription":"23 p. ill., folded map ;29 cm.","costCenters":[],"links":[{"id":106333,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8049.htm","linkFileType":{"id":5,"text":"html"},"description":"8049"},{"id":148178,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1963/0086/report-thumb.jpg"},{"id":43496,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1963/0086/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43497,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1963/0086/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43498,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1963/0086/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43499,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1963/0086/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a917f","contributors":{"authors":[{"text":"Love, J. D.","contributorId":64620,"corporation":false,"usgs":true,"family":"Love","given":"J.","middleInitial":"D.","affiliations":[],"preferred":false,"id":169904,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2744,"text":"wsp1536H - 1963 - Electric analog of three-dimensional flow to wells and its application to unconfined aquifers","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"wsp1536H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1963","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":"1536","chapter":"H","title":"Electric analog of three-dimensional flow to wells and its application to unconfined aquifers","docAbstract":"Electric-analog design criteria are established from the differential equations of ground-water flow for analyzing pumping-test data. A convenient analog design was obtained by transforming the cylindrical equation of flow to a rectilinear form. The design criteria were applied in the construction of an electric analog, which was used for studying pumping-test data collected near Grand Island, Nebr. \r\n\r\nData analysis indicated (1) vertical flow components near pumping wells in unconfined aquifers may be much more significant in the control of water-table decline than radial flow components for as much as a day of pumping; (2) the specific yield during the first few minutes of pumping appears to be a very small fraction of that observed after pumping for more than 1 day; and (3) estimates of specific yield made from model studies seem much more sensitive to variations in assumed flow conditions than are estimates of permeability. Analysis of pumping-test data where vertical flow components are important requires that the degree of anisotropy be known. A procedure for computing anisotropy directly from drawdowns observed at five points was developed. Results obtained in the analog study emphasize the futility of calculating unconfined aquifer properties from pumping tests of short duration by means of equations based on the assumptions that vertical flow components are negligible and specific yield is constant.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1536H","usgsCitation":"Stallman, R., 1963, Electric analog of three-dimensional flow to wells and its application to unconfined aquifers: U.S. Geological Survey Water Supply Paper 1536, iv, 37 p. :ill. ;23 cm., https://doi.org/10.3133/wsp1536H.","productDescription":"iv, 37 p. :ill. ;23 cm.","costCenters":[],"links":[{"id":139040,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1536h/report-thumb.jpg"},{"id":29170,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1536h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a25e4b07f02db60ede1","contributors":{"authors":[{"text":"Stallman, Robert W.","contributorId":32903,"corporation":false,"usgs":true,"family":"Stallman","given":"Robert W.","affiliations":[],"preferred":false,"id":145698,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}