{"pageNumber":"248","pageRowStart":"6175","pageSize":"25","recordCount":6232,"records":[{"id":2483,"text":"wsp1363 - 1956 - Hydrology of Indiana lakes","interactions":[],"lastModifiedDate":"2016-06-21T13:27:34","indexId":"wsp1363","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1956","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":"1363","title":"Hydrology of Indiana lakes","docAbstract":"<p>Indiana's lakes are a valuable resource for both recreational use and their industrial potential. Some lakes are used for water supply.</p>\n<p>The natural lakes are glacial in origin and are most concentrated in northeastern Indiana. Many of the lakes were drained by the early settlers. The natural processes of sedimentation ad accumulation of organic deposits tend also to reduce the number and size of lakes. The trend toward fewer lakes has been reversed in recent years by the construction of artificial lakes; the number of lakes has increased from a little over 500 in 1800 to 1,000 at the present time.</p>\n<p>The recreational value of the lakes and the desirability of maintaining constant lake level led to legislation relative to the establishment of legal lake levels and to a program of lake-level observations, supplemented by the collection of hydrologic data affecting lake levels.</p>\n<p>Observations of both surface temperature and temperature profile were made by investigates as early as 1875. The earlier data and data collected since 1946 have been analyzed to show the fluctuation of temperature with season, depth of water, size of lake, and other influencing factors. Surface temperature, which may vary several degrees within a 24-hour period, fluctuate with air temperature and reach highs of about 85&deg;F in August. The bottom temperature of lakes more than 100 feet deep seldom rise above 45&deg;F. Subsurface water temperatures below ice cover reach a uniform value of about 39&deg;F except that just below the ice which remains closely 32&deg;F. During summer, temperature stratification is established as the lake warms. Shallow lakes reach temperature extremes about 5&deg;F above and below those of deep lakes. Size of the contributing drainage area, surface area of the lake, and flow through the lake have little effect on water temperatures below a depth of about 20 feet. Little aquatic life exists below depths of 30 feet from mid April to mid September owing to a lack of oxygen in the water. Large amounts of cool water, 50 to 10 degrees cooler than groundwater which averages 50&deg;F to 55&deg;F in northern Indiana, are available in the lower portions of the deep lakes.&nbsp;</p>\n<p>Evapotranspiration accounts for the disposal of about 70 percent of the precipitation in Indiana. During a year's time evaporation from the lake surface about equals the precipitation falling on the lake. During dry periods evaporation from a lake may exceed the inflow from small drainage areas and cause a lowering of lake levels. For the period April through October, evaporation as measure in a class A land pan of the U. S. Weather Bureau has averaged 44 inches at Evansville, 34 inches at Indianapolis, and 31 inches at Valpariso. A coefficient of about 0.7 is usually applied to yearly evaporation data from Class A land pans to obtain equivalent evaporation from lake surfaces.</p>\n<p>Ice cover on the lakes extends from about December 15 to March 15 and reaches thickness of 24 to 30 inches during colder winters. Ice can be damaging to the lakeside installations by thrust action of by the wind action on ice cakes.</p>\n<p>The stabilization of lake levels often requires the construction of outlet control structures. A detailed study of past lake-level elevations and other hydologic date is necessary to establish a level that can be maintained and to determine the means necessary for maintaining the established level. Detailed lake-level records for 28 lakes are included in the report, and records for over 100 other lakes data are available in the U.S. Geological Survey Office, Indianapolis, Ind. Evaporation data from the four Class A evaporation station of the U. S. Weather Bureau have been compiled in this report. A table showing the established legal lake level and related data is included.</p>","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1363","usgsCitation":"Perrey, J.I., and Corbett, D.M., 1956, Hydrology of Indiana lakes: U.S. Geological Survey Water Supply Paper 1363, xi, 347 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1363.","productDescription":"xi, 347 p. :ill. ;24 cm.","startPage":"1","endPage":"347","numberOfPages":"360","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":138767,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1363/report-thumb.jpg"},{"id":28577,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1363/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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,{"id":70185482,"text":"70185482 - 1956 - Data and understanding","interactions":[],"lastModifiedDate":"2017-03-22T14:03:02","indexId":"70185482","displayToPublicDate":"1956-01-01T00:00:00","publicationYear":"1956","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Data and understanding","docAbstract":"<p>In the year 1534 when Cabeza de Vaca escaped from the aborigines of southern Texas by whom he had been enslaved for six years, he made his way on foot from the vicinity of Galveston to the west coast of Mexico. Although his <i>Relación</i> was not printed until 1542, the verbal report of Cabeza de Vaca gave impetus to the growing interest in exploration of New Spain. Estevanico, the black, one of de Vaca's companions, served as guide to Fray Marcos de Niza on the first Spanish reconnaissance to reach the village of Zuni in New Mexico.</p><p>The earliest Spanish exploring parties hoped to find riches, but expected to acquire, at the least, facts. These \"gentlemen of high quality,\" as Castaneda called them, wanted to see for themselves whether the cities of Cibola had streets of silver. Hearsay was not enough. Rumor was to be replaced by first-hand knowledge.</p><p>Without discounting the hope for personal gain, these men presumably were fired with some further intellectual and spiritual motivation, among which must have been the desire for facts about these parts where we are assembled. Inscription Rock, only a few miles west of Albuquerque, bears illuminating tidbits of history. Don Diego de Vargas, says the carved inscription of 1692, came here \"A su costa\"—at his own expense.</p><p>We are attempting to survey and correlate some of the facts which people have gained about the nature of semi-arid lands. We are better off than the early Spanish explorers, for in the intervening period data and information have been accumulated in scope and in detail beyond the imagination of our predecessors. We have available excellent maps, knowledge of the soils and of the rocks, both at the surface and below the ground, measurements of precipitation, descriptions of the vegetation, data on the flow of streams, experience in the use, if not the husbandry, of the land.</p><p>It is true that for the purposes of our complex civilization, the need for additional data has far outstripped the programs of fact-finding. But it appears that an indefinite expansion of the collection of routine measurements would still leave something lacking. I draw the distinction between measurement data and understanding; between the collection of facts and knowledge of processes and interrelationships. Although we have a wealth of data, our understanding of the semi-arid environment is poor.</p><p>Understanding the physical and biologic processes operating in an environment is important for living in and with the land. As an example, let us look briefly at the interrelation of the water and sediment in ephemeral streams, and the problem of valley trenching or arroyo cutting.</p>","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"The future of arid lands: Papers and recommendations from the International Arid Lands Meetings","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"International Arid Lands Meetings","conferenceDate":"April 26 - May 4, 1955","conferenceLocation":"Albuquerque, NM","language":"English","publisher":"American Association for the Advancement of Science","publisherLocation":"Washington, D.C.","doi":"10.1002/aic.690030425","usgsCitation":"Leopold, L.B., 1956, Data and understanding, <i>in</i> The future of arid lands: Papers and recommendations from the International Arid Lands Meetings, v. 43, Albuquerque, NM, April 26 - May 4, 1955, p. 114-120, https://doi.org/10.1002/aic.690030425.","productDescription":"7 p.","startPage":"114","endPage":"120","costCenters":[],"links":[{"id":338080,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"43","noUsgsAuthors":false,"publicationDate":"2004-06-17","publicationStatus":"PW","scienceBaseUri":"58d38d66e4b0236b68f98f9a","contributors":{"editors":[{"text":"White, Gilbert F.","contributorId":189688,"corporation":false,"usgs":false,"family":"White","given":"Gilbert","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":685700,"contributorType":{"id":2,"text":"Editors"},"rank":1}],"authors":[{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":685699,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":2784,"text":"wsp1295 - 1955 - Chemical quality of surface waters in Devils Lake basin, North Dakota","interactions":[],"lastModifiedDate":"2018-03-16T13:46:22","indexId":"wsp1295","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1955","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":"1295","title":"Chemical quality of surface waters in Devils Lake basin, North Dakota","docAbstract":"Devils Lake basin, a closed basin in northeastern North Dakota, covers about 3,900 square miles of land, the topography of which is morainal and of glacial origin. In this basin lies a chain of waterways, which begins with the Sweetwater group and extends successively through Mauvais Coulee, Devils Lake, East Bay Devils Lake, and East Devils Lake, to Stump Lake. In former years when lake levels were high, Mauvais Coulee drained the Sweetwater group and discharged considerable water into Devils Lake. Converging coulees also transported excess water to Stump Lake. For at least 70 years prior to 1941, Mauvais Coulee flowed only intermittently, and the levels of major lakes in this region gradually declined. Devils Lake, for example, covered an area of about 90,000 acres in 1867 but had shrunk to approximately 6,500 acres by 1941. Plans to restore the recreational appeal of Devils Lake propose the dilution and eventual displacement of the brackish lake water by fresh water that would be diverted from the Missouri River. Freshening of the lake water would permit restocking Devils Lake with fish. \r\n\r\nDevils and Stump Lake have irregular outlines and numerous windings and have been described as lying in the valley of a preglacial river, the main stem and tributaries of which are partly filled with drift. Prominent morainal hills along the south shore of Devils Lake contrast sharply with level farmland to the north. The mean annual temperature of Devils Lake basin ranges between 36 ? and 42 ? F. Summer temperatures above 100 ? F and winter temperatures below -30 ? Fare not uncommon. The annual precipitation for 77 years at the city of Devils Lake averaged 17.5 inches. Usually, from 75 to 80 percent of the precipitation in the basin falls during the growing season, April to September. \r\n\r\nFrom 1867 to 1941 the net fall of the water surface of Devils Lake was about 38 feet. By 1951 the surface had risen fully 14 feet from its lowest altitude, 1,400.9 feet. Since 1951, the level has fallen slowly. Hydrologic changes that may have caused Devils Lake to alter from a very large, moderately deep lake of fresh water to a small, shallow body of brackish water are discussed and evaluated on the basis of scanty information. During several years of average precipitation, temperature, and evaporation, Devils Lake and lakes upstream should receive nearly a quarter of an inch of runoff annually from the drainage area of about 3,000 square miles. Approximately 55 square miles of tributary area would be required to maintain each square mile of lake surface. However, runoff, expressed as percentage of the average, differs greatly from year to year. The amount of runoff retained in upstream lakes also Varies greatly. For these two reasons, annual inflow to Devils Lake is extremely variable. \r\n\r\nBecause many waterways in this basin have no surface outlets at normal stages, runoff collects in depressions, is concentrated by evaporation, and forms saline or alkaline lakes. The chemical and physical properties of the lake waters vary chiefly with changes in lake stage and volume of inflow. Scattered records from 1899 to 1923 and more comprehensive data from 1948 to 1952 show a range of salt concentration from 6,130 to 25,000 parts per million (ppm) in the water of Devils Lake. Although concentration has varied, the chemical composition of the dissolved solids has not changed appreciably. Lake waters are more concentrated in the lower part of the basin, downstream from Devils Lake. For periods of record the salt concentration ranged from 14,932 to 62,000 ppm in East Devils Lake and from 19,000 to 106,000 ppm in east Stump Lake. \r\n\r\nCurrent and past tonnages of dissolved solids in Devils Lake, East Bay Devils Lake, East Devils Lake, and east and west Stump Lakes were computed from concentrations and from altitude-capacity curves for each lake. Neither the average rate of diversion of water to restore Devils Lake to a higher level nor the quality of the divert","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1295","usgsCitation":"Swenson, H., and Colby, B.R., 1955, Chemical quality of surface waters in Devils Lake basin, North Dakota: U.S. Geological Survey Water Supply Paper 1295, Report: v, 81 p.; Plate: 17.5 x 17.1 inches, https://doi.org/10.3133/wsp1295.","productDescription":"Report: v, 81 p.; Plate: 17.5 x 17.1 inches","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":29259,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1295/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138861,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1295/report-thumb.jpg"},{"id":29258,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1295/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e332f","contributors":{"authors":[{"text":"Swenson, Herbert","contributorId":54181,"corporation":false,"usgs":true,"family":"Swenson","given":"Herbert","affiliations":[],"preferred":false,"id":145781,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Colby, Bruce R.","contributorId":59775,"corporation":false,"usgs":true,"family":"Colby","given":"Bruce","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":145782,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":2845,"text":"wsp1298 - 1955 - Reconnaissance of geology and ground water in the lower Grand River valley, South Dakota, with a section on Chemical quality of the ground water","interactions":[],"lastModifiedDate":"2016-04-05T09:11:18","indexId":"wsp1298","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1955","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":"1298","title":"Reconnaissance of geology and ground water in the lower Grand River valley, South Dakota, with a section on Chemical quality of the ground water","docAbstract":"<p>The area described in this report is the flood plain of the Grand River and the bordering benchlands in Perkins and Corson Counties, S. Dak., from a point about 6 miles west of the town of Shadehill to the confluence of the Grand and Missouri Rivers near Mobridge.</p>\n<p>The exposed bedrock formations include the Pierre shale, the Fox Hills sandstone, and the Hell Creek formation of Late Cretaceous age, and-the Ludlow member of the Fort Union formation of Tertiary (Paleocene) age. Some stringers of the Cannonball formation probably interfinger with beds of the Ludlow member but none of the former was identified during the field investigations. The Pierre shale is exposed from the mouth of the Grand River to approximately the center of the area. Although a few wells in the area obtain water from this formation, it is not generally considered to be a source of supply. The Fox Hills sandstone, the Hell Creek formation, and the Ludlow member of the Fort Union formation are exposed successively upstream and, where saturated, yield small to moderate quantities of water to wells.</p>\n<p>Unconsolidated deposits of silt, sand, and gravel occur in several physiographic positions; they underlie the high benchland on both sides of the river, the poorly defined terraces along the river, and the flood plain throughout its entire length. Possibly all these unconsolidated deposits are water bearing; however, where the deposits on the benchland and in the terraces are dissected by streams, they probably contain little or no water.</p>\n<p>The average depth to ground water along the lower Grand River valley is about 17 feet. Probably, the flow of ground water in the bottom lands is nearly parallel to and slightly toward the surface stream. The measurements of the water level in observation wells for the period 1946-48 indicate that the fluctuations of the water table are small.</p>\n<p>The results of analyses of 13 samples of ground water from the alluvium and the Hell Creek formation show that the suitability of the ground water for use varies because of the considerable range in mineralization and composition. Dissolved solids ranged from 343 to 4,250 parts per million (ppm), hardness from 11 to 1,130 ppm, and percentage of sodium from 25 to 98. Concentrations of some of the individual constituents exceed standards of the United States Public Health Service. The water is moderately hard and contains undesirable amounts of iron and moderate to large amounts of dissolved solids. In general, the water quality ranges from excellent to unsuitable for irrigation use. The result of the mixing of the ground water with recharge water from Shadehill Reservoir cannot be predicted on the basis of available data.</p>\n<p>The geologic and hydrologic data in this report were obtained from earlier reports and from field observations during the period 1946-48. The report includes a geologic map and tabulated well records.</p>","language":"English","publisher":"U.S. Government Print Office","publisherLocation":"Washington, DC","doi":"10.3133/wsp1298","usgsCitation":"Tychsen, P.C., Vorhis, R., and Jochens, E.R., 1955, Reconnaissance of geology and ground water in the lower Grand River valley, South Dakota, with a section on Chemical quality of the ground water: U.S. Geological Survey Water Supply Paper 1298, Report: iv, 33 p.; 2 Plates: 30.00 x 18.15 inches and 27.50 x 9.69 inches, https://doi.org/10.3133/wsp1298.","productDescription":"Report: iv, 33 p.; 2 Plates: 30.00 x 18.15 inches and 27.50 x 9.69 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":138696,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1298/report-thumb.jpg"},{"id":29415,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1298/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29416,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1298/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29417,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1298/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","otherGeospatial":"Grand River Valley","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -102.23876953125,\n              45.336701909968106\n            ],\n            [\n              -102.23876953125,\n              45.73685954736049\n            ],\n            [\n              -100.30517578125,\n              45.73685954736049\n            ],\n            [\n              -100.30517578125,\n              45.336701909968106\n            ],\n            [\n              -102.23876953125,\n              45.336701909968106\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a69e4b07f02db63c389","contributors":{"authors":[{"text":"Tychsen, Paul C.","contributorId":82683,"corporation":false,"usgs":true,"family":"Tychsen","given":"Paul","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":145896,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vorhis, R.C.","contributorId":32512,"corporation":false,"usgs":true,"family":"Vorhis","given":"R.C.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":145894,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jochens, Eugene R.","contributorId":55804,"corporation":false,"usgs":true,"family":"Jochens","given":"Eugene","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":145895,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":1162,"text":"wsp1357 - 1955 - Computations of total sediment discharge, Niobrara River near Cody, Nebraska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:12","indexId":"wsp1357","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1955","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":"1357","title":"Computations of total sediment discharge, Niobrara River near Cody, Nebraska","docAbstract":"A natural chute in the Niobrara River near Cody, Nebr., constricts the flow of the river except at high stages to a narrow channel in which the turbulence is sufficient to suspend nearly the total sediment discharge. Because much of the flow originates in the sandhills area of Nebraska, the water discharge and sediment discharge are relatively uniform. \r\n\r\nSediment discharges based on depth-integrated samples at a contracted section in the chute and on streamflow records at a recording gage about 1,900 feet upstream are available for the period from April 1948 to September 1953 but are not given directly as continuous records in this report. Sediment measurements have been made periodically near the gage and at other nearby relatively unconfined sections of the stream for comparison with measurements at the contracted section. \r\n\r\nSediment discharge at these relatively unconfined sections was computed from formulas for comparison with measured sediment discharges at the contracted section. A form of the Du Boys formula gave computed tonnages of sediment that were unsatisfactory. Sediment discharges as computed from the Schoklitsch formula agreed well with measured sediment discharges that were low, but they were much too low at measured sediment discharges that were higher. The Straub formula gave computed discharges, presumably of bed material, that were several times larger than measured discharges of sediment coarser than 0.125 millimeter. All three of these formulas gave computed sediment discharges that increased with water discharges much less rapidly than the measured discharges of sediment coarser than 0.125 millimeter. \r\n\r\nThe Einstein procedure when applied to a reach that included 10 defined cross sections gave much better agreement between computed sediment discharge and measured sediment discharge than did anyone of the three other formulas that were used. This procedure does not compute the discharge of sediment that is too small to be found in the stream bed in appreciable quantities. Hence, total sediment discharges were obtained by adding computed discharges of sediment larger than 0.125 millimeter to measured discharges of sediment smaller than 0.125 millimeter. The size distributions of the computed sediment discharge compared poorly with the size distributions of sediment discharge at the contracted section. Ten sediment discharges computed from the Einstein procedure as applied to a single section averaged several times the measured sediment discharge for the contracted section and gave size distributions that were unsatisfactory.\r\n\r\nThe Einstein procedure was modified to compute total sediment discharge at an alluvial section from readily measurable field data. The modified procedure uses measurements of bed-material particle sizes, suspended-sediment concentrations and particle sizes from depth-integrated samples, streamflow, and water temperatures. Computations of total sediment discharge were made by using this modified procedure, some for the section at the gaging station and some for each of two other relatively unconfined sections. The size distributions of the computed and the measured sediment discharges agreed reasonably well. Major advantages of this modified procedure include applicability to a single section rather than to a reach of channel, use of measured velocity instead of water-surface slope, use of depth-integrated samples, and apparently fair accuracy for computing both total sediment discharge and approximate size distribution of the sediment. Because of these advantages this modified procedure is being further studied to increase its accuracy, to simplify the required computations, and to define its limitations. \r\n\r\nIn the development of the modified procedure, some relationships concerning theories of sediment transport were reviewed and checked against field data. Vertical distributions of suspended sediment at relatively unconfined sections did not agree well with theoretical dist","language":"ENGLISH","publisher":"U.S. Geological Survey ; for sale by U.S. G.P.O.,","doi":"10.3133/wsp1357","isbn":"pbk","usgsCitation":"Colby, B.R., and Hembree, C., 1955, Computations of total sediment discharge, Niobrara River near Cody, Nebraska: U.S. Geological Survey Water Supply Paper 1357, vii, 187 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1357.","productDescription":"vii, 187 p. :ill. ;24 cm.","costCenters":[],"links":[{"id":137363,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1357/report-thumb.jpg"},{"id":25989,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25990,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25991,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25992,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25993,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25994,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25995,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1357/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25996,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1357/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a6392","contributors":{"authors":[{"text":"Colby, Bruce R.","contributorId":59775,"corporation":false,"usgs":true,"family":"Colby","given":"Bruce","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143282,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hembree, C. H.","contributorId":106866,"corporation":false,"usgs":true,"family":"Hembree","given":"C. H.","affiliations":[],"preferred":false,"id":143283,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70047728,"text":"70047728 - 1955 - Sediment investigations of the Platte River near Overton, Nebraska","interactions":[],"lastModifiedDate":"2013-12-17T10:21:58","indexId":"70047728","displayToPublicDate":"1949-01-19T16:06:00","publicationYear":"1955","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"title":"Sediment investigations of the Platte River near Overton, Nebraska","docAbstract":"<p>This report contains results of sediment-transport investigations on the Platte River near Overton,. Nebr. from January 1950 to September 1953. The basic data of suspended-sediment studies, results of bed-material analyses, and determinations of water-surface slopes from staff readings are given.</p>\n<br/>\n<p>The data indicate that a reliable determination of suspended sediment, hence total load, is difficult. Because of the nature of the river at the station and the limited scope of the investigations, the suspended-sediment data may not be representative. </p>\n<br/>\n<p>The Platte River is characterized by a wide braided channel, a small hydraulic radius, low banks, and a wide flood plain. (See figs. 1 and 2.,) The river bed is composed of coarse to fine sands. </p>\n<br/>\n<p>Near Overton, natural flow of the river is controlled or modified by diversions, storage reservoirs, power development, return flow from irrigation, and withdrawals of ground water. A temporary jetty was extended into the river below the bridge during the summer of 1952 as part of commercial sand pumping operations. Beavers carry on active construction in the narrows and shallows, particularly upstream from the sampling section. </p>\n<br/>\n<p>Daily fluctuations in water discharge at the gaging station at the bridge are caused by regulation of the flow, mainly from the generation of power by release of water from a reservoir The water discharge at the station begins increasing about 9:30 a.m., reaches a crest about 2:00 p.m and then immediately recede. Weekly water-discharge measurements of alternate high and low stages indicate a daily variation from 200 to more than 1,000 cfs. During spring summer, and fall increases in water dis charge are also caused by thunderstorm activity in the area.</p>","language":"English","publisher":"U.S. Geological Survey Water Resources","doi":"10.3133/70047728","collaboration":"Prepared as part of a program of the Department of the Interior for development of the Missouri River basin","usgsCitation":"Albert, C., and Guy, H., 1955, Sediment investigations of the Platte River near Overton, Nebraska, 37 p., https://doi.org/10.3133/70047728.","productDescription":"37 p.","numberOfPages":"40","temporalStart":"1950-01-01","temporalEnd":"1953-09-30","costCenters":[{"id":629,"text":"Water Resources Division","active":false,"usgs":true}],"links":[{"id":276824,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70047728/report-thumb.jpg"},{"id":279946,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70047728/report.pdf"}],"country":"United States","state":"Nebraska","otherGeospatial":"Platte River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -99.7838,40.6372 ], [ -99.7838,40.7742 ], [ -99.1901,40.7742 ], [ -99.1901,40.6372 ], [ -99.7838,40.6372 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"52148fe5e4b06d85e08fb51b","contributors":{"authors":[{"text":"Albert, C.D.","contributorId":23923,"corporation":false,"usgs":true,"family":"Albert","given":"C.D.","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":482834,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Guy, H.P.","contributorId":73571,"corporation":false,"usgs":true,"family":"Guy","given":"H.P.","email":"","affiliations":[],"preferred":false,"id":482835,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70175976,"text":"70175976 - 1954 - Geology and ground-water resources of Wichita and Greeley Counties, Kansas","interactions":[],"lastModifiedDate":"2017-04-18T16:19:24","indexId":"70175976","displayToPublicDate":"2015-12-08T00:00:00","publicationYear":"1954","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2579,"text":"Kansas Geological Survey Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Geology and ground-water resources of Wichita and Greeley Counties, Kansas","docAbstract":"<p>This report describes the geography, geology, and ground-water resources of Wichita and Greeley counties in western Kansas. The area consists of a flat to gently rolling plain, which slopes eastward [at] about 15 feet per mile. A short reach of Ladder Creek (Beaver) is the only perennially flowing stream in the two counties. Ephemeral streams, which flow only during and after heavy rains, are White Woman and Sand Creeks and the western reach of Ladder Creek. The climate is semiarid, the normal annual precipitation being about 17 inches in Wichita County and 16 inches in Greeley County. Agriculture is the principal occupation in the area, and wheat is the most important crop. A considerable area is irrigated; sugar beets and sorghums are the principal irrigated crops.</p><p>The outcropping rocks range in age from late Cretaceous to Recent; the Smoky Hill chalk member of the Niobrara formation, which is exposed along White Woman Creek in western Greeley County, is the oldest. The Niobrara is almost everywhere overlain by the Ogallala formation of Pliocene age. Generally the Ogallala is overlain by windblown silt of the Pleistocene Sanborn formation, but in places it is exposed along streams. The most recent deposits are dune sand and the alluvium along the streams. The Dakota formation, which is an important aquifer in parts of Kansas, is 300 to 450 feet beneath the Niobrara formation.</p><p>The ground water that is available to wells in Wichita and Greeley counties is derived entirely from precipitation in the area or in areas immediately west and north. Ground water moves in a generally easterly direction with a gradient that varies inversely with the permeability of the water-bearing beds. The ground-water reservoir is recharged principally by precipitation within the area or within adjacent areas, Ground-water discharge takes place principally by pumping from wells, subsurface outflow, and evaporation and transpiration. Most of the domestic, stock, public, and irrigation supplies are obtained from wells. It is estimated that probably more than 2 billion gallons of water is pumped annually from wells in the area. Since 1947, ground-water recharge has been about equal to ground-water discharge.</p><p>The use of ground water for irrigation has increased greatly since 1946 and indications are that many more wells may be drilled and pumped without dangerously lowering the water table. Approximately 11,000 to 12,000 acres were irrigated in 1951. A map showing the thickness of water-bearing materials indicates that although much of the area has enough water-bearing material to support irrigation wells, parts of Wichita and Greeley counties have little or none.</p><p>The Ogallala is the principal water-bearing formation in the area. Small amounts of water may also be obtained locally from alluvial deposits and from cracks in the Niobrara formation. Two deep test wells to the Dakota formation have been drilled but, because of the poor quality of the water, have never been used.</p><p>The ground water in Wichita and Greeley counties, though hard, is suitable for most purposes. Water from the Ogallala is generally high in fluoride and in some cases may be injurious to the teeth of children. Water from the Dakota, though soft, is unfit for irrigation because of a high content of sodium.</p><p>The field data upon which most of this report is based are given in tables; they include records of 417 wells, chemical analyses of 31 samples of water, and logs of 57 test holes and wells.</p>","language":"English","publisher":"University of Kansas","publisherLocation":"Lawrence, KS","usgsCitation":"Prescott, G., Branch, J., and Wilson, W., 1954, Geology and ground-water resources of Wichita and Greeley Counties, Kansas: Kansas Geological Survey Bulletin, v. 108, 134 p. .","productDescription":"134 p. ","costCenters":[{"id":353,"text":"Kansas Water Science Center","active":false,"usgs":true}],"links":[{"id":327505,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":327503,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.kgs.ku.edu/General/geologyBulls.html"}],"volume":"108","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57bd73dbe4b03fd6b7df2ce9","contributors":{"authors":[{"text":"Prescott, G.C. Jr.","contributorId":103352,"corporation":false,"usgs":true,"family":"Prescott","given":"G.C.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":646733,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Branch, J.R.","contributorId":173971,"corporation":false,"usgs":false,"family":"Branch","given":"J.R.","email":"","affiliations":[],"preferred":false,"id":646734,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wilson, W.W.","contributorId":6396,"corporation":false,"usgs":true,"family":"Wilson","given":"W.W.","email":"","affiliations":[],"preferred":false,"id":646735,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":51617,"text":"ofr5427 - 1954 - Floods in Devils and Pecos River basins of Texas, June 27-28, 1954 - miscellaneous data","interactions":[],"lastModifiedDate":"2016-08-09T14:43:51","indexId":"ofr5427","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1954","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":"54-27","title":"Floods in Devils and Pecos River basins of Texas, June 27-28, 1954 - miscellaneous data","docAbstract":"<p>Record-breaking floods occurred June 27, 28, 1954, in the Devils and lower Pecos Rivers and in some tributaries to those streams, caused by heavy rainfall of June 26-28. At the time of the flood the geological Survey was not operating a gaging station in the Devils River basin or in the Pecos river basin below Girvin. Continuous records of the flow of Devils River were obtained by the Geological Survey at the station at Baker's Crossing near Juno from May 1925 to September 1949 and on the Pecos River near Sheffield from October 1921 to April 1925 and from October 1939 to September 1949. Records of the great flood flows near the mouths of the Devils and Pecos Rivers mentioned above were obtained by the International Boundary and Water Commission, United States and Mexico, at gaging stations maintained by that agency on the Devils River near Del Rio and the Pecos River near Comstock. The outstanding nature of the flood in the lower Pecos River is shown by the fact that the maximum stage reached at the Comstock gaging station was 97.8 ft on June 27, 1954, whereas the maximum stage reached at this gage between the beginning of record in 1900 and 1954 was only 38.2 ft.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5427","usgsCitation":"Breeding, S., 1954, Floods in Devils and Pecos River basins of Texas, June 27-28, 1954 - miscellaneous data: U.S. Geological Survey Open-File Report 54-27, 8 p., https://doi.org/10.3133/ofr5427.","productDescription":"8 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":178399,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr5427.jpg"},{"id":310477,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1954/0027/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Texas","otherGeospatial":"Devils River, Pecos River","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -101.00006103515625,\n              30.20567424070585\n            ],\n            [\n              -101.08245849609375,\n              30.185496022109444\n            ],\n            [\n              -101.13189697265625,\n              30.148689804618368\n            ],\n            [\n              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,{"id":51292,"text":"ofr53121 - 1953 - Fifth progress report on the cooperative investigation of springs and streamflow in the Tecolote Tunnel area of Santa Barbara County, California","interactions":[],"lastModifiedDate":"2024-08-06T14:09:42.939311","indexId":"ofr53121","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1953","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":"53-121","title":"Fifth progress report on the cooperative investigation of springs and streamflow in the Tecolote Tunnel area of Santa Barbara County, California","docAbstract":"<p>This report is the fifth in a continuing series of annual progress reports giving the results of discharge measurements made at more than 120 selected sites in the \"Tecolote Tunnel Area\" of the Santa Ynez Mountains. This area derives its name from the tunnel now being built by the Bureau of Reclamation for the purpose of diverting the flood waters of the Santa Ynez River as stored in Cachuma Reservoir to the city of Santa Barbara and adjacent coastal communities. The tunnel alignment is roughly north and south through the center of this area, which extends from Refugio Pass on the west to San Marcos Pass and the Painted Cave area on the east.</p><p>The program of measuring the developed springs and headwater streams in the Tecolote Tunnel area was started on its present scale in the latter part of 1948 at the request of the Santa Barbara County Water Agency. The primary purpose of the program is to obtain sufficient factual data to determine what effect, if any, the construction and use of the Tecolote Tunnel will have on the outflow of the springs in the area. The area covered by this study was made large enough to include all springs that could possibly be affected by the tunnel, as well as springs believed to be outside the zone of influence. The program is being carried on by the Geological Survey under a cooperative agreement with the Santa Barbara County Water Agency whereby each pays one half the cost.</p><p>Prior to January 1953 the flow at each of the more than 120 locations was generally measured monthly. Since then, the number of sites at which monthly measurements are made has been reduced to about 40, with measurements made every other month or quarterly at the remaining locations. The purpose of this report is to make available the factual data obtained from May 1, 1952 to June 30, 1953.</p>","language":"English","doi":"10.3133/ofr53121","collaboration":"Prepared in cooperation with the Santa Barbara County Water Agency","usgsCitation":"Hofmann, W., 1953, Fifth progress report on the cooperative investigation of springs and streamflow in the Tecolote Tunnel area of Santa Barbara County, California: U.S. Geological Survey Open-File Report 53-121, Report: 156 p.; 1 Plate: 25.52 x 19.41 inches, https://doi.org/10.3133/ofr53121.","productDescription":"Report: 156 p.; 1 Plate: 25.52 x 19.41 inches","costCenters":[],"links":[{"id":432279,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1953/0121/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":179365,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1953/0121/report-thumb.jpg"},{"id":432278,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1953/0121/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"50000","country":"United States","state":"California","county":"Santa Barbara County","otherGeospatial":"Tecolote Tunnel","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -120.61474653419313,\n              35.107477322182945\n            ],\n            [\n              -120.61474653419313,\n              33.603227658961316\n            ],\n            [\n              -119.21258359397822,\n              33.603227658961316\n            ],\n            [\n              -119.21258359397822,\n              35.107477322182945\n            ],\n            [\n              -120.61474653419313,\n              35.107477322182945\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fbe4b07f02db5f497c","contributors":{"authors":[{"text":"Hofmann, Walter","contributorId":30604,"corporation":false,"usgs":true,"family":"Hofmann","given":"Walter","email":"","affiliations":[],"preferred":false,"id":243277,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3541,"text":"cir274 - 1953 - Water resources of the Minneapolis-St. Paul area, Minnesota","interactions":[],"lastModifiedDate":"2022-10-26T21:24:06.323848","indexId":"cir274","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1953","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"274","title":"Water resources of the Minneapolis-St. Paul area, Minnesota","docAbstract":"<p>The water supply of the Minneapolis-St. Paul area is adequate to satisfy present requirements and requirements for many years to come if the area continues to develop at about the present rate.</p>\n<p>The flow of -the Mississippi River at the Twin Cities is more than sufficient to meet the demands of the water-supply systems of Minneapolis and St. Paul. The lowest momentary flow during the period 1931-51 was more than twice the present combined maximum demand of Minneapolis and St. Paul. The lake storage of the St. Paul system combined with possible regulations by the Mississippi River headwater reservoir system, in case of an emergency, provides a reserve supply ample to meet a greatly expanded demand. The lowest average daily flow of the Mississippi River at the intakes of the Minneapolis and St. Paul water supply was 389 mgd (602 cfs), The flow at the water supply intakes has been less than 452 mgd (700 cfs) for not more than 6 consecutive days.</p>\n<p>Except for the Mississippi River, the streams in the Twin Cities area have not been extensively developed for water supply. The only known use of them for water supply is for the steam-electric. generating plant on the Minnesota River at Savage. Thus, the St. Croix River, within 12 miles on the east, the Minnesota River entering the Twin Cities from the southwest, the Vermilion within 12 miles on the south, and the Crow River within 25 miles on the west offer untapped supplies for industrial and municipal uses.</p>\n<p>Many water-bearing formations occur in the area. A blanket of glacial deposits, as much as 400 feet thick, covers the area. Small domestic ground-water supplies can be developed practically everywhere in the glacial deposits, and larger industrial supplies can be obtained by exploring and testing. Below the glacial materials is a thick series of rock formations including several prolific sandstone aquifers. The formations dip toward the center of the area forming an artesian basin.</p>\n<p>The estimated average daily withdrawal of ground water from all aquifers in the area is about 90 mgd. Practically all the communities that are not supplied by the Minneapolis or St. Paul water-supply systems obtain their water from wells.</p>\n<p>Where many large-capacity wells have been concentrated in relatively small areas, there has been a great lowering of artesian pressures. However, there are large areas, distant from the centers of concentrated pumping, which are favorable for the development of additional ground water. With an adequate program of exploration and testing to determine precisely the geologic and hydrologic characteristics of the waterbearing formations, it is likely that large additional supplies of ground water can be developed for municipal and industrial uses.</p>\n<p>Both Minneapolis and St. Paul obtain their municipal water supplies from the Mississippi River above the TwinCities and are thus assured of a large supply that is not subject to contamination by industrial wastes and sewage effluents, Treatment at municipal plants for both cities provides water for diversified industrial use and for domestic use that meets U. S. Public Health Service drinking water standards., The treated water is remarkably uniform in chemical composition throughout the year and is virtually free of all color, iron, manganese, and turbidity. Currently, (1952). the two supplies are softened to about 75 ppm (as CaC03), which is an average reduction of about 55 percent in hardness of river water. The dissolvedsolids content of the treated water for St. Paul currently (1952) averages about 100 ppm; the dissolved-solids content of the Minneapolis water is slightly higher. As a matter of further interest to industrial consumers, temperatures of the untreated river water, which is only slightly altered at the Minneapolis treatment plant, averages less than 60 F for about 8 months of the year and is less than 40 F for 4 winter months.</p>\n<p>The Mississippi River as it enters the Twin Cities is moderately mineralized, averaging 241 ppm dissolved solids and 179 ppm hardness during the period 1940-49, Average turbidity is very low and silica is moderately low, but the quantities of iron and color in solution are relatively high. Color increases markedly during the period March to July in response to an increase in streamflow. The average chemical composition of the water has remained virtually unchanged except for seasonal variations since 1907.</p>\n<p>Data collected by the Minneapolis-St. Paul Sanitary District have shown improved sanitary conditions of the river at the Twin Cities lock and dam since the sewage plant went into operation in 1939.</p>\n<p>The Minnesota River is more than twice as mineralized and hard as the Mississippi River, and it exerts a noticeable effect on the chemical and sanitary quality of the Mississippi River at St. Paul.</p>\n<p>Other principal tributary streams to the Mississippi River, including Crow River, Vermilion River, and Bassett Creek, were sampled during the 1952 flood season, at which time they were of the calcium-bicarbonate type, more dilute, and of lower hardness than the Minnesota River. Lake waters in the Twin Cities area generally are less mineralized than those of the streams.</p>\n<p>Waters from the drift deposits and bedrock formations overlying the Hinckley sandstone are hard and calcareous and generally contain troublesome quantities of iron. Regular treatment is required of some public-supply wells for removal of iron encrustations. Water fr.om these sources generally exceeds 300 ppm hardness, but in some places the St. Peter sandstone and St. Lawrence formation yield water of better quality. The Hinckley sandstone yields the best quality ground-water because of its comparatively lower hardness and uniform temperature (about 52 F). However, the average hardness of the treated municipal supplies of St. Paul and Minneapolis is considerably less than water from the Hinckley.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/cir274","collaboration":"Based on data collected in cooperation with the Minnesota Department of Conservation, Division of Waters and St. Paul District, Corps of Engineers, U. S. Army","usgsCitation":"Prior, C.H., Schneider, R., and Durum, W.H., 1953, Water resources of the Minneapolis-St. Paul area, Minnesota: U.S. Geological Survey Circular 274, Report: 49 p.; 3 Plates: 22.00 x 16.94 inches or smaller, https://doi.org/10.3133/cir274.","productDescription":"Report: 49 p.; 3 Plates: 22.00 x 16.94 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":408780,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_23664.htm","linkFileType":{"id":5,"text":"html"}},{"id":30559,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1953/0274/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30558,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/1953/0274/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30557,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/1953/0274/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":126443,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1953/0274/report-thumb.jpg"},{"id":247311,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/1953/0274/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","city":"Minneapolis, St. Paul","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -93.76968383789062,\n              44.630550504861795\n            ],\n            [\n              -93.76968383789062,\n              45.298075138707965\n            ],\n            [\n              -92.73971557617188,\n              45.298075138707965\n            ],\n            [\n              -92.73971557617188,\n              44.630550504861795\n            ],\n            [\n              -93.76968383789062,\n              44.630550504861795\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602c54","contributors":{"authors":[{"text":"Prior, Charles Henry","contributorId":6839,"corporation":false,"usgs":true,"family":"Prior","given":"Charles","email":"","middleInitial":"Henry","affiliations":[],"preferred":false,"id":147126,"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":147128,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Durum, W. H.","contributorId":78311,"corporation":false,"usgs":true,"family":"Durum","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":147127,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":50,"text":"wsp1137F - 1953 - Floods of November-December 1950 in the Central Valley basin, California","interactions":[],"lastModifiedDate":"2023-01-12T21:56:03.437077","indexId":"wsp1137F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1953","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":"1137","chapter":"F","title":"Floods of November-December 1950 in the Central Valley basin, California","docAbstract":"The flood of November-December 1950 in the Central Valley basin was the greatest in most parts of the basin since the turn of the century and probably was exceeded in the lower San Joaquin River basin only by the historic flood of 1862. In respect to monetary loss, the 1950 flood was the most disastrous in the history of the basin. Loss of life was remarkably small when one considers the extensive damage and destruction to homes and other property, which is estimated at 33 million dollars. Outstanding features of the flood were its unprecedented occurrence so early in the winter flood season, its magnitude in respect to both peak and volume in most major tributaries, and the occurrence of a succession of near-peak flows with a period of three weeks. \r\n\r\nThe flood was caused by a series of storms during the period November 16 to December 8, which brought exceptionally warm, moisture-laden air inland against the Sierra Nevada range and caused intense rainfall, instead of snowfall, at unusually high altitudes. Basin-wide totals of rainfall during the period ranged from 30 inches over the Yuba and American River basins to 13 inches over the upper Sacramento and Feather River basins. \r\n\r\nBased on continuous records of discharge on major tributaries for periods ranging from 22 to 55 years and averaging about 43 years, the 1950 flood peaks were the greatest of record on the American, Cosumnes, Mokelumne, Stanislaus, Tuolumne, Merced, Chowchilla, Fresno, lower San Joaquin, Kings, Kaweah, Tule, and Kern Rivers. Second highest peak of record occurred during the flood of March 1928 on the Yuba, American and Mokelumne Rivers; the flood of Marcn 1940 on Cosumnes River; the flood of January 1911 on the Stanislaus and Tuolumne Rivers; the flood of December 1937 on the Merced, Kings, and Kaweah Rivers; the flood of March 1938 on the Chowchilla, Fresno, and lower San Joaquin Rivers; and the flood of March 1943 on the Tule and Kern Rivers. Peak discharges for 1950 did not exceed previous maxima on Bear, Yuba, Feather, and upper Sacramento Rivers, nor on west side tributaries of lower Sacramento River, Calaveras River, and upper San Joaquin River (above Friant Reservoir). \r\n\r\nNotable high rates of discharge were 354 cfs per square mile from 39.5 square miles in North Fork of Middle Fork Tule River, 225 cfs per square mile from 198 square miles in Rubicon River, 115 cfs per square mile from 999 square miles in North Fork of American River and 93.7 cfs per square mile from 1,921 square miles in American River at Fair Oaks. \r\n\r\nThis report presents a general description of the 1950 flood, details and estimates of the damage incurred, records of stage and discharge for the period of the flood at 171 stream-gaging stations, records of storage in 14 reservoirs, a summary of peak discharges with comparative data for previous floods at 252 measurement points, and tables showing crest stages along the main stem and major tributary channels of the Sacramento and San Joaquin Rivers. \r\n\r\nThe report also includes a discussion of meteorologic and hydrologic conditions associated with the flood, examples of the flood regulation afforded by storage reservoirs, a brief study of runoff characteristics, and a summary and comparison with previous floods in the Central Valley basin.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1137F","usgsCitation":"Paulsen, C.G., 1953, Floods of November-December 1950 in the Central Valley basin, California: U.S. Geological Survey Water Supply Paper 1137, Report: ix, 85 p.; 6 Plate: 29.00 x 35.50 inches or smaller, https://doi.org/10.3133/wsp1137F.","productDescription":"Report: ix, 85 p.; 6 Plate: 29.00 x 35.50 inches or smaller","costCenters":[],"links":[{"id":411810,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24230.htm","linkFileType":{"id":5,"text":"html"}},{"id":24687,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1137f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":24686,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1137f/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":24685,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1137f/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":24684,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1137f/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":24683,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1137f/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":24682,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1137f/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":24681,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1137f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137395,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1137f/report-thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Central Valley basin","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -119.00217681950107,\n              35.13952919516764\n            ],\n            [\n              -118.44677630187559,\n              36.447316753430925\n            ],\n            [\n              -120.27199477688288,\n              38.169213736701124\n            ],\n            [\n              -121.83334007970987,\n              40.062197180496526\n            ],\n            [\n              -121.87363587923997,\n              40.74570155104911\n            ],\n            [\n              -122.73875148861515,\n              40.49630948575876\n            ],\n            [\n              -122.72263734102694,\n              39.539602288586565\n            ],\n            [\n              -121.46737875338653,\n              37.74605097908976\n            ],\n            [\n              -120.18232868135271,\n              36.10951673244216\n            ],\n            [\n              -119.33641582011342,\n              35.142729172215766\n            ],\n            [\n              -119.00217681950107,\n              35.13952919516764\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d8e4b07f02db5df882","contributors":{"authors":[{"text":"Paulsen, C. G.","contributorId":96239,"corporation":false,"usgs":true,"family":"Paulsen","given":"C.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":141874,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":57707,"text":"ofr53289 - 1953 - Changes in chemical quality of the Arkansas River in Oklahoma and Arkansas (1946-52)","interactions":[],"lastModifiedDate":"2012-02-02T00:12:29","indexId":"ofr53289","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1953","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":"53-289","title":"Changes in chemical quality of the Arkansas River in Oklahoma and Arkansas (1946-52)","docAbstract":"Systematic chemical quality-of-water investigations have been carried on in both Oklahoma and Arkansas by the Geological Survey in cooperation with State and Federal agencies during the past several years. Results of the Survey's quality-of-water investigations are usually published in the annual Water-Supply Papers. However, as the Geological Survey has made no sediment investigations in the Arkansas River Basin in Oklahoma and Arkansas, the published data do not include information on sediment concentrations or loads.\r\nThis report attempts to summarize information collected to date in the Arkansas River Basin of the two States, and to show as clearly as possible from present information how the chemical quality of water in the Arkansas River changes downstream from the Oklahoma-Kansas State line to its confluence with the Mississippi River, and how it is affected by tributary inflows. Additional information is being collected and further studies are planned. Hence, the conclusions reached herein may be modified by more adequate information at a later date.\r\n\r\nThe Arkansas River enters Oklahoma near Newkirk on the northern boundary just east of the 97th meridian, crosses the State in a general southeasterly direction flowing past Tulsa, enters Arkansas at its western boundary north of the 35th parallel near Fort Smith, still flowing in a general southeasterly direction past Little Rock near the center of the State, and empties into the Mississippi River east of Dumas.\r\n\r\nThe Arkansas River is subject to many types of pollution downstream from the Oklahoma-Kansas State line, and its inferior quality along with an erratic flow pattern has caused it to be largely abandoned as a source of municipal and industrial water supply. At the present time, the Arkansas River is not directly used as a source of public supply in any part of the basin in either Oklahoma or Arkansas. In general, the river water increases in chemical concentration downstream from the Oklahoma-Kansas State line to Tulsa, due mainly to tributary inflow from the Salt Fork Arkansas River and the Cimarron River, both streams being sources of large amounts of both natural and artificial pollution. A decrease in chemical concentration is noted downstream from Tulsa due to tributary inflow from the Verdigris, Neosho, and Illinois rivers with an increase in chemical concentration then noted due to tributary inflow from the Canadian River which is largely artificial pollution. A steady decrease in concentration is then noted as the river progresses through Arkansas to the Mississippi River, as all major tributaries below the Canadian River have a dilution effect upon the chemical concentration of the Arkansas River water.\r\n\r\nProposals for storage and regulating reservoirs on the Arkansas River in both Oklahoma and Arkansas have been made by the Corps of Engineers and others. Additional proposals are being considered in the present Arkansas-White-Red River Basin Inter-Agency Committee studies. If constructed, these reservoirs will provide an opportunity for control of flow and beneficial use of Arkansas River water, both at and downstream from these sites. Impoundment alone will greatly reduce the extremes in water quality, and by reasonable control of municipal and industrial wastes, the water would be comparable in quality to many existing basin municipal and industrial supplies.\r\n\r\n(available as photostat copy only)","language":"ENGLISH","doi":"10.3133/ofr53289","usgsCitation":"Dover, T., and Geurin, J., 1953, Changes in chemical quality of the Arkansas River in Oklahoma and Arkansas (1946-52): U.S. Geological Survey Open-File Report 53-289, 33 p., https://doi.org/10.3133/ofr53289.","productDescription":"33 p.","costCenters":[],"links":[{"id":182938,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cee4b07f02db5455ef","contributors":{"authors":[{"text":"Dover, T.B.","contributorId":90293,"corporation":false,"usgs":true,"family":"Dover","given":"T.B.","email":"","affiliations":[],"preferred":false,"id":257624,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Geurin, J.W.","contributorId":59784,"corporation":false,"usgs":true,"family":"Geurin","given":"J.W.","affiliations":[],"preferred":false,"id":257623,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":57706,"text":"ofr53288 - 1953 - Summary of annual records of chemical quality of water of the Arkansas River in Oklahoma and Arkansas, 1945-1952","interactions":[],"lastModifiedDate":"2012-02-02T00:12:29","indexId":"ofr53288","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1953","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":"53-288","title":"Summary of annual records of chemical quality of water of the Arkansas River in Oklahoma and Arkansas, 1945-1952","docAbstract":"This report summarizes information collected to date in the Arkansas River Basin in Oklahoma and Arkansas, and shows, within the limitations of present information, the chemical quality of water in the Arkansas River downstream from the Oklahoma-Kansas State line to its junction with the Mississippi River, and the influence of tributary in-flows. Additional data are being collected and further studies are planned. Hence, conclusions reached herein may be modified by more complete information at a later date.\r\nThe Arkansas River is subject to many types of pollution downstream from the Oklahoma-Kansas State line, and its inferior quality along with an erratic flow pattern has caused it to be largely abandoned as a source of municipal and industrial water supply. Currently, the Arkansas River is not directly used as a source of public supply in any part of the basin in either Oklahoma or Arkansas. In general, the river water increases in chemical concentration downstream from the Oklahoma-Kansas State line to Tulsa due mainly to tributary inflow from the Salt Fork Arkansas River and the Cimarron River, both streams being sources of large amounts of both natural salts and industrial wastes. A decrease in chemical concentration is noted downstream from Tulsa due to tributary inflow from the Verdigris, Neosho, and Illinois rivers, with an increase in chemical concentration then noted due to tributary inflow from the Canadian River which is largely oil field wastes. A steady decrease in concentrations is then noted as the river progresses through Arkansas to the Mississippi River, as all major tributaries below the Canadian River have a dilution effect upon the chemical concentration of the Arkansas River water.\r\n\r\nProposals for storage and regulating reservoirs on the Arkansas River in both Oklahoma and Arkansas have been made by the Corps of Engineers and others. Additional proposals are bing considered in the present Arkansas-White-Red River Basin Inter-Agency Sub-Committee studies. If constructed, these reservoirs will provide an opportunity for control of flow and beneficial use of Arkansas River water both at and downstream from these sites. Impoundment alone will greatly reduce the extremes in water-quality, and by reasonable control of municipal and industrial wastes, the water at some points on the river would be comparable in quality to many existing municipal and industrial supplies in the basin.\r\n\r\n(available as photostat copy only)","language":"ENGLISH","doi":"10.3133/ofr53288","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1953, Summary of annual records of chemical quality of water of the Arkansas River in Oklahoma and Arkansas, 1945-1952: U.S. Geological Survey Open-File Report 53-288, 38 leaves ; 28 cm., https://doi.org/10.3133/ofr53288.","productDescription":"38 leaves ; 28 cm.","costCenters":[],"links":[{"id":182937,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db6982f7","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":533178,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":13965,"text":"ofr172 - 1952 - Ground water in the Gila River Basin and adjacent areas, Arizona: a summary","interactions":[],"lastModifiedDate":"2018-08-29T08:13:56","indexId":"ofr172","displayToPublicDate":"2013-08-04T14:49:00","publicationYear":"1952","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":"172","title":"Ground water in the Gila River Basin and adjacent areas, Arizona: a summary","docAbstract":"<p>This report is a resume' of the principal facts collected by the Geological Survey in the period 1890-1952 about the ground-water resources of the Gila River basin and certain other areas in Arizona. Since 1939 the Geological Survey has been making ground-water investigations on a continuing basis in cooperation with the State of Arizona. Since 1940 the cooperating agency has been the State Land Department.</p><p>The occurrence of ground water in fifteen areas that form a part of the Gila River drainage basin is described in this report. The areas are denoted by the name of a town or geographic feature, and are as follows: Duncan, Safford, San Simon, Upper San Pedro, Lower San Pedro, Aravaipa Creek, Upper Santa Cruz, Lower Santa Cruz, Salt River Valley, Rainbow ValleyWaterman Wash, McMullen Valley, Harquahala Plain, Gila Bend, Palomas Plain, and Wellton-Mohawk. Data also are presented for several areas not in the Gila River system, including Ranegras Plain and the Willcox and Douglas basins. A summary of the data is given following the ground-water discussion in each area.</p><p>A series of maps accompany the report, including an index map and maps of the principal areas of ground-water development. The mar,z, show the geology, the location of most of the irrigation wells and irrigated lands, and, where data were available, contours of the water table, depth to the water table, and changes in its position over a period of years.</p><p>Ground water occurs in the region primarily in alluvial fill consisting of gravel, sand, silt, and clay which was deposited in structural troughs between mountain ranges. Ground water stored in these alluvial basins is derived from many sources. The principal sources are infiltration from runoff along the mountain fronts and seepage from irrigation water applied to cultivated lands.</p><p>Of great interest in Arizona at the present time is the rate of depletion of ground-water reserves by withdrawals from storage. Use of ground water in Arizona increased by more than 50 percent in the 6-year period 1'46-51, from 2,400,000 acre-feet in 1946 to 3,750,000 acre-feet in 1951. The areas of greatest withdrawal are in Pinal and Maricopa Counties, in the southcentral part of the State. Maps and hydrographs accompanying this report show that the water table is declining in the heavily pumped areas, indicating that ground water is being withdrawn in excess of replenishment. The rate of decline has been as much as 10 feet per year in the most intensively pumped areas, and has been greatest during the past few years.</p><p>In an effort to compensate for decreased well yields resulting from the decline of the water table in some areas, many deep wells have been drilled within the past few years. The deep aquifers do not represent a new source of water; their water is a part of the common supply of the structural basins in which they lie. The aquifers tapped by these deep wells generally yield less water per foot of drawdown than the shallower aquifers. The water in the deeper aquifers is variable in quality, ranging from water too high in dissolved solids to be usable for irrigation to water lower in concentration than that in the overlying aquifers.</p><p>The quality of the ground waters in most of the region is considered suitable for irrigation. In local areas, however, the ground waters are naturally unsuitable for irrigation and, in other areas, the concentration of dissolved solids has increased sufficiently to make the waters harmful to some crops. The problem of salt balance is becoming increasingly important, not only in the Salt River Valley area, but also in other parts of the Gila River Basin. A discussion of the salt-balance problem is given in Part II of this report.&nbsp;</p><p>It should be emphasized that ground waters in each of the individual areas in the Gila River drainage system are interrelated with ground waters in adjacent areas upstream and downstream. The connection is tenuous between some areas, but in central Arizona the ground waters in the different areas are closely related. Although subsurface barriers to ground-water movement exist in places, they are not everywhere fully effective.</p><p>The ground-water--surface-water interrelationship is important in some areas. Those basins occupied by perennial streams, or by streams having large influent seepage losses, have not shown large, perennial declines of water levels in wells. Effluent seepage of ground water contributes to stream flow in the lower reaches of several basins. </p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr172","usgsCitation":"Halpenny, L.C., 1952, Ground water in the Gila River Basin and adjacent areas, Arizona: a summary: U.S. Geological Survey Open-File Report 172, xxii, 224 p., https://doi.org/10.3133/ofr172.","productDescription":"xxii, 224 p.","costCenters":[],"links":[{"id":356900,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/0172/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":291630,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/0172/report-thumb.jpg"}],"country":"United States","state":"Arizona","otherGeospatial":"Gila River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -114.5581,32.6315 ], [ -114.5581,33.3923 ], [ -108.2049,33.3923 ], [ -108.2049,32.6315 ], [ -114.5581,32.6315 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53e09e59e4b0beb42bdca43a","contributors":{"authors":[{"text":"Halpenny, Leonard Cameron","contributorId":66698,"corporation":false,"usgs":true,"family":"Halpenny","given":"Leonard","email":"","middleInitial":"Cameron","affiliations":[],"preferred":false,"id":168710,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3550,"text":"cir182 - 1952 - Evaluation of streamflow records in Flathead River basin, Montana","interactions":[],"lastModifiedDate":"2013-07-29T14:11:58","indexId":"cir182","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1952","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"182","title":"Evaluation of streamflow records in Flathead River basin, Montana","docAbstract":"This report presents data which are, in general, supplementary to those of the surface-water investigations made in the past by the Geological Survey. Those investigations have consisted essentially of the operation of the many gaging stations on the Flathead River and tributaries. The data presented were obtained from a detailed field investigation of the various manmade devices that are factors influencing the quantity or regimen of the flow at the gaging stations. These factors include diversions from the stream, bypass channels carrying water around the gaging stations, return flow from irrigation or other projects, storage and release of flood waters, and other similar factors. Where feasible, the location, size, effect upon the streamflow, periods of use, method of operation, and similar information are given. The information is segregated into sections corresponding to areas determined by the location of gaging stations. An index of streamflow records is included.  A section dealing with the adequacy of .available water-resources data, including location and period of record, also is included. This information is given in general terms only, and is portrayed mainly by maps and graphs.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/cir182","usgsCitation":"Plunkett, R., 1952, Evaluation of streamflow records in Flathead River basin, Montana: U.S. Geological Survey Circular 182, Report: iv, 30 p.; 1 Map: 12.46 x 18.73 inches, https://doi.org/10.3133/cir182.","productDescription":"Report: iv, 30 p.; 1 Map: 12.46 x 18.73 inches","costCenters":[],"links":[{"id":126699,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/0182/report-thumb.jpg"},{"id":30570,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/0182/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271082,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/0182/plate-1.pdf"}],"country":"United States","state":"Montana","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -116.05,44.36 ], [ -116.05,49.0 ], [ -104.04,49.0 ], [ -104.04,44.36 ], [ -116.05,44.36 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a06e4b07f02db5f8bf4","contributors":{"authors":[{"text":"Plunkett, R.T.","contributorId":107266,"corporation":false,"usgs":true,"family":"Plunkett","given":"R.T.","email":"","affiliations":[],"preferred":false,"id":147144,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":51102,"text":"ofr5221 - 1952 - Fourth progress report on the cooperative investigation of springs and streamflow in the Tecolote Tunnel area of Santa Barbara County, California","interactions":[],"lastModifiedDate":"2024-08-06T14:15:03.635194","indexId":"ofr5221","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1952","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":"52-21","title":"Fourth progress report on the cooperative investigation of springs and streamflow in the Tecolote Tunnel area of Santa Barbara County, California","docAbstract":"<p>This is a continuation of annual progress reports giving the results of discharge measurements made in the Santa Ynez Mountains between Refugio Canyon on the west to San Marcos Pass and the Painted Cave area on the east. This portion of Santa Barbara County has been designated as the \"Tecolote Tunnel Area\" because a tunnel by that name, now being built by the Bureau of Reclamation, passes through it. The purpose of this tunnel is to divert flood runoff from the Santa Ynez River, stored in Cachuma Reservoir, to the city of Santa Barbara and adjacent areas.</p><p>During the construction of this tunnel, the seepage from the south portal has averaged 6.4 second-feet for the year ending April 30, 1952, the average being 8.7 second-feet for the last 6 months of that period. Both of these values exceed the average total discharge prior to April 30, 1951, for more than 120 springs measured in the Tecolote Tunnel Area.</p><p>As, it was not known what effect the seepage from this tunnel might have on the flow of springs and streams in the immediate vicinity, the Santa Barbara County Water Agency requested the U. S. Geological Survey to institute an observational program. This program was started in 1948—about 2 years before work was started on the tunnel. The area covered by the observational program was made sufficiently large to include all the springs that could possibly be affected, as well as certain border springs believed to be outside the zone of influence.</p><p>The purpose of this, the fourth progress report, is to make available factual data obtained during the year ending April 30, 1952. This program is operated under a cooperative agreement between the U. S. Geological Survey and the Santa Barbara County Water Agency whereby each pays half the cost of the investigation.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5221","collaboration":"Prepared in cooperation with the Santa Barbara County Water Agency","usgsCitation":"Burgess, C., 1952, Fourth progress report on the cooperative investigation of springs and streamflow in the Tecolote Tunnel area of Santa Barbara County, California: U.S. Geological Survey Open-File Report 52-21, Report: 156 p.; 1 Plate: 25.61 x 19.26 inches, https://doi.org/10.3133/ofr5221.","productDescription":"Report: 156 p.; 1 Plate: 25.61 x 19.26 inches","costCenters":[],"links":[{"id":432282,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1952/0021/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":432281,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1952/0021/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":178379,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1952/0021/report-thumb.jpg"}],"scale":"50000","country":"United States","state":"California","county":"Santa Barbara County","otherGeospatial":"Tecolote Tunnel","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -120.61474653419313,\n              35.107477322182945\n            ],\n            [\n              -120.61474653419313,\n              33.603227658961316\n            ],\n            [\n              -119.21258359397822,\n              33.603227658961316\n            ],\n            [\n              -119.21258359397822,\n              35.107477322182945\n            ],\n            [\n              -120.61474653419313,\n              35.107477322182945\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a9099","contributors":{"authors":[{"text":"Burgess, C.E.","contributorId":64329,"corporation":false,"usgs":true,"family":"Burgess","given":"C.E.","email":"","affiliations":[],"preferred":false,"id":242957,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3366,"text":"cir129 - 1952 - Hydrologic reconnaissance of the Green River in Utah and Colorado","interactions":[{"subject":{"id":52980,"text":"ofr5099 - 1950 - Hydrologic reconnaissance of the Green River in Utah and Colorado","indexId":"ofr5099","publicationYear":"1950","noYear":false,"title":"Hydrologic reconnaissance of the Green River in Utah and Colorado"},"predicate":"SUPERSEDED_BY","object":{"id":3366,"text":"cir129 - 1952 - Hydrologic reconnaissance of the Green River in Utah and Colorado","indexId":"cir129","publicationYear":"1952","noYear":false,"title":"Hydrologic reconnaissance of the Green River in Utah and Colorado"},"id":1}],"lastModifiedDate":"2017-02-21T15:52:17","indexId":"cir129","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1952","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"129","title":"Hydrologic reconnaissance of the Green River in Utah and Colorado","docAbstract":"<p>The Green River, rising in Wyoming and draining high mountains in that state, northeast Utah and northwest Colorado, is a major tributary of the Colorado River. In the late summer, after the snow has melted from these mountains, the flow in the Green River reaches its minimum for the year. At that time a large proportion of the water in the river is returned to the atmosphere by evaporation and transpiration.</p><p>During a 21-day period in September 1948, when the flow was least for the year, the average flow of the river as it entered Utah from Wyoming was 515 cfs. In the 437 miles of its course through Utah and Colorado evapotranspiration losses averaged 430 cfs. The average discharge of the Green River into the Colorado was about 975 cfs. Contributions to the river in Utah and Colorado totalled 890 cfsi including 560 from tributaries. The calculated ground-water inflow was about 330 cfs, of which about 75 percent was contributed within the Uinta Basin. Verv little ground water was contributed to the river in the lower 180 miles of its course, where the river flows through canyon lands of the Colorado Plateaus.</p><p>These estimates are based upon information collected during a boat reconnaissance in September 1948, and upon data available from stream-gaging stations along the Green River and many of its tributaries. From these data an accounting was made of the water--as to both quantity and quality--in several segments of the river. For each segment determinations were made of the surface outflow, loss by evapotranspiration, and surface- and ground-water inflow. During the reconnaissance information was also obtained as to the relation of stream flow to regional geology and ground-water hydrology.</p><p>No detailed hydrologic studies have yet been made within the drainage basin of the Green River. On the basis of this recomiaissance, detailed studies in the Uinta Basin, Browns Park, and Echo Park areas are recommended as highly desirable, because of the possible relations of ground-water hydrology to river-basin development projects. Similar reconnaissance can be of value in delineating the areas where detailed hydrologic studies would be most fruitful throughout the upper Colorado River basin.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/cir129","usgsCitation":"Thomas, H.E., 1952, Hydrologic reconnaissance of the Green River in Utah and Colorado: U.S. Geological Survey Circular 129, Report: iv, 32 p.; 1 Plate: 13.88 x 13.42 inches, https://doi.org/10.3133/cir129.","productDescription":"Report: iv, 32 p.; 1 Plate: 13.88 x 13.42 inches","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":30376,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/0129/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138602,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/0129/report-thumb.jpg"},{"id":271087,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/0129/report.pdf"}],"country":"United States","state":"Colorado, Utah","otherGeospatial":"Green River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -0.01638888888888889,8.333333333333334E-4 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.016666666666666666,0.0011111111111111111 ], [ -0.016666666666666666,8.333333333333334E-4 ], [ -0.01638888888888889,8.333333333333334E-4 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a18e4b07f02db605548","contributors":{"authors":[{"text":"Thomas, H. E.","contributorId":12829,"corporation":false,"usgs":true,"family":"Thomas","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":146729,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":51090,"text":"ofr528 - 1952 - Memorandum on the ground-water resources of the Horse Creek and Cherry Creek drainage basins, Wyoming","interactions":[],"lastModifiedDate":"2019-08-21T13:04:01","indexId":"ofr528","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1952","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":"52-8","title":"Memorandum on the ground-water resources of the Horse Creek and Cherry Creek drainage basins, Wyoming","docAbstract":"<p>This report is one of several that are being made by the United States Geological Survey as part of the program of the Department of the Interior for the control, conservation, development, and use of the water resources of the Missouri River basin. The purpose of this report is to present an annotated bibliography of all existing reports pertaining to ground-water supplies in the area reported upon; to collect and analyze all data on public, industrial, and irrigation pumping from wells that are not covered by previous reports; to indicate areas where additional large-scale pumping might be undertaken; to estimate the possibility of depletion of stream flow by ground-water pumping from the developed areas and from areas where large-scale pumping maybe undertaken in the future; to point out areas where aquifers might be artificially recharged; and to recommend areas where detailed ground-water studies should be made, indicating the studies needed.</p><p>The writer spent approximately 2 weeks in the field during June 1952 evaluating the results of previous studies to determine their adequacy with respect to the purpose of this report. It was found that the previous studies in the area adequately covered the ground-water conditions for this purpose; consequently, the following discussion is abstracted largely from reports covering those studies. </p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr528","collaboration":"Compiled as part of program of Interior Department for development of the Missouri River Basin","usgsCitation":"Babcock, H.M., 1952, Memorandum on the ground-water resources of the Horse Creek and Cherry Creek drainage basins, Wyoming: U.S. Geological Survey Open-File Report 52-8, ii, 12 p., https://doi.org/10.3133/ofr528.","productDescription":"ii, 12 p.","costCenters":[{"id":5050,"text":"WY-MT Water Science Center","active":true,"usgs":true}],"links":[{"id":86449,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1952/0008/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":178995,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1952/0008/report-thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"Horse Creek and Cherry Creek Drainage Basins","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -106.55639648437499,\n              41.008920735004885\n            ],\n            [\n              -104.0625,\n              41.008920735004885\n            ],\n            [\n              -104.0625,\n              42.9524020856897\n            ],\n            [\n              -106.55639648437499,\n              42.9524020856897\n            ],\n            [\n              -106.55639648437499,\n              41.008920735004885\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a2ce4b07f02db613f86","contributors":{"authors":[{"text":"Babcock, H. M.","contributorId":90698,"corporation":false,"usgs":true,"family":"Babcock","given":"H.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":242916,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3524,"text":"cir187 - 1952 - Evaluation of streamflow records in Rogue River basin, Oregon","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"cir187","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1952","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"187","title":"Evaluation of streamflow records in Rogue River basin, Oregon","docAbstract":"This report presents data which are, in general, supplementary to those the surface-water investigations made in the past by the U. S. Geological Survey. Those have been essentially investigations of the operation of the many gaging stations on the Rogue River and tributaries. \r\n\r\nThe data presented were obtained from a detailed field investigation of the various #actors resulting from man-made structures that influence the quantity or regimen of the flow at the gaging stations. These factors include diversions from the stream, bypass channels carrying water around the gaging stations, return flow from irrigation or other projects, storage and release of flood waters, and other similar factors. Where feasible, the location, size, effect upon the streamflow periods of use, method of operation,, and similar information are. given. The information is divided into sections corresponding to areas determined by the location of gaging stations. An index of streamflow records is included. \r\n\r\nA section dealing with the adequacy of available water-resources data and containing location and period of record also is included. This information is given in general terms only, and is portrayed mainly by maps and graphs.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/cir187","usgsCitation":"Richardson, D., 1952, Evaluation of streamflow records in Rogue River basin, Oregon: U.S. Geological Survey Circular 187, iv, 48 p. :ill., maps (1 fold. in pocket) ;27 cm., https://doi.org/10.3133/cir187.","productDescription":"iv, 48 p. :ill., maps (1 fold. in pocket) ;27 cm.","costCenters":[],"links":[{"id":123009,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1952/0187/report-thumb.jpg"},{"id":30538,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/1952/0187/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30539,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1952/0187/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a06e4b07f02db5f887d","contributors":{"authors":[{"text":"Richardson, Donald","contributorId":68288,"corporation":false,"usgs":true,"family":"Richardson","given":"Donald","email":"","affiliations":[],"preferred":false,"id":147089,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":51156,"text":"ofr5298 - 1952 - Geology and hydrology of dam sites on the island of St. Croix, Virgin Islands","interactions":[],"lastModifiedDate":"2024-07-10T18:23:33.828929","indexId":"ofr5298","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1952","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":"52-98","title":"Geology and hydrology of dam sites on the island of St. Croix, Virgin Islands","docAbstract":"<p>The Virgin Islands Corporation plans to build a series of small earth dams along some of the streams on the island of St. Croix, and field studies involving the selection and hydrology of possible sites was carried on by the Geological Survey during the months of August and September 1951. The island of St. Croix is the largest of the three principal islands of the Virgin. Islands group owned by the United States. It is about 21 miles long and 6 miles wide near the center and has an area of about 84 square miles. The northwestern part of the island contains mountains that reach a maximum altitude of 1,165 feet; the eastern half of the island is submountainous, containing some hills 600 to 800 feet in altitude. A coastal lowland area containing a few east-west trending marl and limestone hills characterizes the southwestern part of the island. The streams in the east half of the island and along the northwest coast are relatively short and are dry during most of the year. The streams draining the mountains from the south cross the coastal lowland in narrow and shallow ditches. The southeastward drainage from the eastern part of the mountainous area is diverted by Salt River and enters the sea on the north coast of the island. In the headwaters of some streams there is a small flow of water during most of the year that disappears below the surface upstream from or near the foot of the mountains. During most of the year the streams are essentially dry, flowing only after periods of heavy rainfall.</p><p>In the coastal lowland near Bethlehem the average annual rainfall is about 46 inches. The east end of the island is relatively dry and the precipitation is estimated to be approximately 20 inches annually; the northwestern end of the island receives the most rainfall, probably more than 50 inches annually. Records show that from 1861 to 1876 there was deficient rainfall and the accumulated departure below normal was about 56 inches (fig. 2). From 1876 to 1920 there were numerous years of above -normal precipitation and the departure curve rose nearly 100 inches, to more than 40 inches above normal. From 1936 to 1950 there has been a more or less continuous decline in rainfall, amounting to a net deficiency of 72 inches, or from 44 inches above to 28 inches below normal. These changes in rainfall have a direct effect on the volume of stream flow an island.</p><p>There are two general rock types on the island. The Mount Eagle volcanics and the intruded diorite are hard, dense crystalline rocks; the rock's underlying the coastal lowland and belt of hills between Salt River and Christiansted are sedimentary rocks, such as marl, limestone, sand, gravel, and clay. The permeability of the crystalline rocks and of the gray clay and basal conglomerate of the Jealousy formation is low and they are water bearing in few places. The Kingshill formation is composed of light-gray clay and light-yellow marl and included beds of limestone. In places the limestone contains solutional openings that yield water to wells. The alluvial sand, gravel, and clay that unconformably overlie the Kingshill marl include permeable beds that yield relatively large quantities of water to wells in a few places.</p><p>It is evident from the small stream flow that by far the greatest part of the 46-inch average annual precipitation on the island is returned to the atmosphere through evaporation and transpiration. There are no records of stream flaw or ground-water flow from the drainage basins, but it is estimated that in some years the amount of water lost through evaporation and transpiration may be more than 90 percent of the total water available. It is proposed that a program be started and continued to collect and evaluate data on the hydrology of the island.</p><p>The purpose of the dam-building program is to retain on the land a part of the water that formerly flowed to the sea and was of no beneficial use. Owing to the lack of hydrologic data, the maximum number of dams needed is not known; consequently, practically all possible sites on publicly owned land and sites that would benefit those lands were studied. Thus, 3 sites were selected in the valley near Little Grange that is a source of supply to the public-supply well field of Frederiksted; 19 sites were selected on or near property owned by the Virgin Islands Corporation; and 4 sites were selected along the Salt River above the public-supply well field of Christiansted. During most of the year the water table is at or below the beds of the streams; consequently, if permeable rocks underlie a pond or dam it is possible that there may be leakage from the pond to the water table. In general, leakage from dam sites underlain by crystalline rocks of the fount Eagle volcanics or clay of the Kingshill marl will be negligible, but leakage from sites underlain by limestone in the Kingshill marl or sand and gravel of the alluvium may be great. Potential leakage at each site selected is discussed.</p>","language":"English","doi":"10.3133/ofr5298","collaboration":"Prepared in cooperation with the Office of Territories United States Department of the Interior","usgsCitation":"Meyer, R.R., 1952, Geology and hydrology of dam sites on the island of St. Croix, Virgin Islands: U.S. Geological Survey Open-File Report 52-98, 67 p., https://doi.org/10.3133/ofr5298.","productDescription":"67 p.","costCenters":[],"links":[{"id":430902,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1952/0098/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":177166,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1952/0098/report-thumb.jpg"}],"country":"United States","state":"Virgin Islands","otherGeospatial":"St. Croix","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -64.91293924634013,\n              17.802398867836004\n            ],\n            [\n              -64.91293924634013,\n              17.65497511341303\n            ],\n            [\n              -64.56284831047668,\n              17.65497511341303\n            ],\n            [\n              -64.56284831047668,\n              17.802398867836004\n            ],\n            [\n              -64.91293924634013,\n              17.802398867836004\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b4671","contributors":{"authors":[{"text":"Meyer, R. R.","contributorId":20725,"corporation":false,"usgs":true,"family":"Meyer","given":"R.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":243065,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70217842,"text":"70217842 - 1952 - Discussion of “tide‐producing forces and artesian pressures”","interactions":[],"lastModifiedDate":"2021-02-05T18:44:33.420843","indexId":"70217842","displayToPublicDate":"1952-08-01T12:40:56","publicationYear":"1952","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1578,"text":"Eos, Transactions, American Geophysical Union","onlineIssn":"2324-9250","printIssn":"0096-394","active":true,"publicationSubtype":{"id":10}},"title":"Discussion of “tide‐producing forces and artesian pressures”","docAbstract":"<p>I was an employee of the Texas State Board of Water Engineers in charge of the Fort Stockton field office at the time that the data for this paper were gathered. Since I have done both extensive and detailed ground‐water work in the Fort Stockton area, including the setting and maintaining of the water‐stage recorder at the Gonzales well, I believe I can add some pertinent hydrologic remarks about this paper.</p><p>The authors state that the principal water‐bearing formation is a limestone. This opinion is not shared by myself and most likely the majority of other geologists in this area. Adkins [1927] favored the basal Cretaceous sands as the principal source of water to Comanche Springs. I believe that the most extensive and the principal water‐bearing formation is a sand and sandstone. The crevices and channels reported in wells and exposed at the springs are only a localized condition resulting from structural weakness and solution caused by a high water surface. The piezometric surface in sand and crevice wells is essentially identical; this suggests that there exists but one principal aquifer in this area. W.N. White, former District Geologist in Texas for the U.S. Geological Survey, in a personal communication to me in 1948, reported Comanche Springs to be the most reliable springs in Texas. This reliable flow strongly supports the concept of a sand aquifer, whose catchment area, or source, is of vast and varied extent, and a great distance from its outlet.</p>","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TR033i004p00597","usgsCitation":"Culbertson, T., George, W., and Romberg, F.E., 1952, Discussion of “tide‐producing forces and artesian pressures”: Eos, Transactions, American Geophysical Union, v. 33, no. 4, p. 597-600, https://doi.org/10.1029/TR033i004p00597.","productDescription":"4 p.","startPage":"597","endPage":"600","costCenters":[],"links":[{"id":383059,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"33","issue":"4","noUsgsAuthors":false,"publicationDate":"2014-08-18","publicationStatus":"PW","contributors":{"authors":[{"text":"Culbertson, Tom","contributorId":248797,"corporation":false,"usgs":false,"family":"Culbertson","given":"Tom","email":"","affiliations":[],"preferred":false,"id":809882,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"George, William O.","contributorId":106016,"corporation":false,"usgs":true,"family":"George","given":"William O.","affiliations":[],"preferred":false,"id":809883,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Romberg, Frederick E.","contributorId":248796,"corporation":false,"usgs":false,"family":"Romberg","given":"Frederick","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":809884,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":3378,"text":"cir96 - 1951 - Ground-water resources of the Paintrock irrigation project, Wyoming, with a section on the quality of the water","interactions":[],"lastModifiedDate":"2022-07-07T21:24:00.785636","indexId":"cir96","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1951","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"96","title":"Ground-water resources of the Paintrock irrigation project, Wyoming, with a section on the quality of the water","docAbstract":"<p>The ground-water conditions of the area covered by the Paintrock irrigation project, in north-central Wyoming, were investigated during the summer of 1947. The purpose of the study was to obtain a general evaluation of ground-water recharge, discharge, and storage in the area now irrigated and in the adjacent areas where additional lands are to be irrigated.</p><p>Much of the area covered by this report consists of flat to gently sloping stream terraces and alluvial-bottoms along Nowood, Paintrock, and Medicine Lodge Creeks. The stream-terrace materials consist of fluviatile sand, clay, and gravel. The alluvium is very fine grained and in general has low permeability. The materials underlying the stream terraces and the bottomlands became progressively finer grained and less permeable downstream.</p><p>The bedrock formations underlying the area studied range from the Madison limestone of Mississippian age to the Fort Union formation of Paleocene age. Beds have been folded into several prominent structures which trend northwest-southeast across the area. Several of the formations exposed in the area serve as aquifers and yield water to domestic and stock wells. The most important bedrock aquifers are the Fort Union, Lance, Meeteetee, Mesaverde, Frontier, Cloverly and Morrison formations , the Tensleep sandstone, the Amsden formation, and the Madison limestone. More than 7,000 feet of strata are exposed in the area, the older beds being exposed on the western flank of the Big Horn Range near the eastern end of the area.</p><p>The quality of the water in the project ranges within wide limits. The concentration of dissolved solids in seven samples of ground water ranges from 279 parts per million for a water in the Tensleep sandstone to 4,590 parts per million for a water in the Morrison formation. The hardness as calcium carbonate (CaCO<sub>3</sub>) ranges from 13 to 1,680 parts per million. Limited data on the quality of water in Nowood and Paintrock Creeks indicate that these waters are suitable for irrigation. The water in Paintrock Creek near Tensleep is higher in mineral content and hardness than the water upstream at Hyattville as a result of return flow of the irrigation water that is applied to farm lands above Tensleep.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir96","usgsCitation":"Swenson, F.A., Bach, W.K., and Swenson, H.A., 1951, Ground-water resources of the Paintrock irrigation project, Wyoming, with a section on the quality of the water: U.S. Geological Survey Circular 96, Report: ii, 45 p.; Plate: 26.50 x 10.60 inches, https://doi.org/10.3133/cir96.","productDescription":"Report: ii, 45 p.; Plate: 26.50 x 10.60 inches","costCenters":[],"links":[{"id":123573,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1951/0096/report-thumb.jpg"},{"id":30391,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1951/0096/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":30390,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/1951/0096/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"},{"id":403240,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_23947.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Wyoming","county":"Big Horn County","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -108.052,\n              44.188\n            ],\n            [\n              -107.497,\n              44.188\n            ],\n            [\n              -107.497,\n              44.312\n            ],\n            [\n              -108.052,\n              44.312\n            ],\n            [\n              -108.052,\n              44.188\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a96e4b07f02db65a852","contributors":{"authors":[{"text":"Swenson, Frank Albert","contributorId":71958,"corporation":false,"usgs":true,"family":"Swenson","given":"Frank","email":"","middleInitial":"Albert","affiliations":[],"preferred":false,"id":146751,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bach, W. Kenneth","contributorId":20312,"corporation":false,"usgs":true,"family":"Bach","given":"W.","email":"","middleInitial":"Kenneth","affiliations":[],"preferred":false,"id":146750,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Swenson, Herbert A.","contributorId":93461,"corporation":false,"usgs":true,"family":"Swenson","given":"Herbert","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146752,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":51036,"text":"ofr5128 - 1951 - Geology and ground-water resources of the northern part of the Ranegras Plain area, Yuma County, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:11:29","indexId":"ofr5128","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1951","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":"51-28","title":"Geology and ground-water resources of the northern part of the Ranegras Plain area, Yuma County, Arizona","docAbstract":"The Ranegras Plain area is part of the Basin and Range province in west-central Arizona.\r\n\r\nThe report discusses rocks of pre-Cambrian, pre-Cambrian (?), Paleozoic (?), Mesozoic (?), Cretaceous (?), Cretaceous and Tertiary, Tertiary (?), Quaternary (?), and Quaternary age. All the Paleozoic (?) and Cretaceous (?) rocks and parts of the Mesozoic (?),Cretaceous and Tertiary, and Tertiary (?) rocks have been mapped as a unit because they are so intensely faulted that detailed mapping was not practical. Rocks older than Quaternary form the mountain ranges bordering the Ranegras Plain. Quaternary alluvium underlies the broad, gently sloping valley floor to depths of generally a few hundred feet, locally more. Well logs indicate that the underlying Tertiary (?) alluvium exceeds 1,100 feet in thickness.\r\n\r\nThe structure of the area is controlled by faulting typical of the Basin and Range province, but the major faults are covered by alluvium and are inferred from topographic features.\r\n\r\nGround water occurs in Quaternary and Tertiary (?) alluvium and the best aquifers are in sand and gravel of the Quaternary alluvium. Ground-water movement is, in general, to the northwest.\r\n\r\nRecharge to the aquifers is predominantly from stream flow resulting from heavy rains. There is also minor or unevaluated recharge from underflow from Butler Valley to the east, and\u0014since 1948\u0014seepage from irrigation.\r\n\r\nDischarge is by pumping and by natural processes of underflow and evapotranspiration. In addition to small domestic and stock wells, only two irrigation wells, in the vicinity of Utting, are in use. No accurate data on pumpage are available.\r\n\r\nThe safe yield from the ground-water reservoir may be less than 5,000 acre-feet and probably does not exceed 10,000 to 15,000 acre-feet per year.\r\n\r\nThe quality of ground water ranges from permissible to unsuitable for irrigation purposes. The fluoride content is generally too high for the water to be considered satisfactory for use by young children.","language":"ENGLISH","doi":"10.3133/ofr5128","usgsCitation":"Metzger, D.G., 1951, Geology and ground-water resources of the northern part of the Ranegras Plain area, Yuma County, Arizona: U.S. Geological Survey Open-File Report 51-28, 31 p. (1 folded) : ill., map ; 27 cm., https://doi.org/10.3133/ofr5128.","productDescription":"31 p. (1 folded) : ill., map ; 27 cm.","costCenters":[],"links":[{"id":179149,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1951/0028/report-thumb.jpg"},{"id":86422,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1951/0028/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86423,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1951/0028/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c99f","contributors":{"authors":[{"text":"Metzger, Donald George","contributorId":36915,"corporation":false,"usgs":true,"family":"Metzger","given":"Donald","email":"","middleInitial":"George","affiliations":[],"preferred":false,"id":242787,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3767,"text":"cir71 - 1950 - Techniques used in mine-water problems of the east Tennessee zinc district","interactions":[],"lastModifiedDate":"2012-02-02T00:05:32","indexId":"cir71","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1950","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"71","title":"Techniques used in mine-water problems of the east Tennessee zinc district","docAbstract":"A study of ground water as related to mining in cavernous limestones and dolomites in eastern Tennessee was made in 1946 by the U. S. Geological Survey. Surface and subsurface mapping indicated the geologic control of underground channels. Several methods of tracing water were tried and new techniques in using these methods evolved from the work. Rainfall data, when correlated with ground-water volumes and velocities, gave much information as to expected pumping volumes for any period. The use of fluorescent dye for tracing the flow of the water is described and other methods are discussed briefly. Four examples, each from a different mine, are discussed in detail and some remedies for the problems are suggested.","language":"ENGLISH","publisher":"[U.S. Geological Survey],","doi":"10.3133/cir71","usgsCitation":"Kent, D.F., 1950, Techniques used in mine-water problems of the east Tennessee zinc district: U.S. Geological Survey Circular 71, 9 p. :ill. ;27 cm., https://doi.org/10.3133/cir71.","productDescription":"9 p. :ill. ;27 cm.","costCenters":[],"links":[{"id":122062,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1950/0071/report-thumb.jpg"},{"id":30832,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1950/0071/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685a8a","contributors":{"authors":[{"text":"Kent, Deane Frederick","contributorId":42083,"corporation":false,"usgs":true,"family":"Kent","given":"Deane","email":"","middleInitial":"Frederick","affiliations":[],"preferred":false,"id":147567,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":3936,"text":"cir74 - 1950 - A glossary of uranium- and thorium-bearing minerals","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"cir74","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1950","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"74","title":"A glossary of uranium- and thorium-bearing minerals","docAbstract":"During 1980, an estimated 121 million gallons of water per day was pumped in a 26-county area in east-central Georgia from sand aquifers of Paleocene and Late Cretaceous age. Maximum withdrawals were at the kaolin mining and processing centers in Twiggs, Wilkinson, and Washington Counties, where water levels have declined as much as 50 ft since 1944-50. In the southern two-thirds of the study area, water levels have shown little, if any, change. Declining water levels and increasing competition for groundwater have caused concern over the adequacy of groundwater supplies. This report defines the areal extent and describes the geohydrology of the Paleocene-Upper Cretaceous aquifers of east-central Georgia, and evaluates the effects of man on the groundwater flow system. Geohydrologic data from four test wells indicate that the aquifers consist of alternating layers of sand and clay that are largely of deltaic origin. In the northern third of the study area, the confining unit between the Dublin and Midville aquifer systems is absent and the aquifer systems combine to form the Dublin-Midville aquifer system. The aquifer systems range in thickness from 80 to 645 ft and their transmissivities range from 800 to 39,000 sq ft/day. The hydraulic conductivity ranges from 15 to 530 ft/day. Wells yield as much as 3,400 gpm (gallons per minute). Chemical analyses of water from 49 wells indicate that water from both aquifer systems is of good quality except in the central part of the study area, where iron concentrations are as high as 6,700 micrograms/L and exceed the 300 micrograms/L recommended limit for drinking water. The principal recharge to the aquifer systems is from precipitation that occurs within and adjacent to the outcrop areas. The principal discharge is to streams in the outcrop area. (Author 's abstract)","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir74","usgsCitation":"Frondel, J.W., and Fleischer, M., 1950, A glossary of uranium- and thorium-bearing minerals: U.S. Geological Survey Circular 74, 20 p. ;27 cm., https://doi.org/10.3133/cir74.","productDescription":"20 p. ;27 cm.","costCenters":[],"links":[{"id":123799,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1950/0074/report-thumb.jpg"},{"id":31021,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1950/0074/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae59e","contributors":{"authors":[{"text":"Frondel, Judith Weiss","contributorId":55810,"corporation":false,"usgs":true,"family":"Frondel","given":"Judith","email":"","middleInitial":"Weiss","affiliations":[],"preferred":false,"id":147856,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fleischer, Michael","contributorId":65835,"corporation":false,"usgs":true,"family":"Fleischer","given":"Michael","email":"","affiliations":[],"preferred":false,"id":147857,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
]}