Two unusually massive ostreid species, representing the largest and youngest Mesozoic members of their respective lineages, occur in Upper Cretaceous sediment of the gulf coast and Caribbean areas. Their characteristics and significance, as well as the morphologic terminology of ostreids in general, are discussed.
\nCrassostrea cusseta Sohl and Kauffman n. sp. is the largest known ostreid from Mesozoic rocks of North America; it occurs sporadically in the Cusseta Sand and rarely in the Blufftown Formation of the Chattahoochee River region in Georgia and Alabama. It is especially notable in that it lacks a detectable posterior adductor muscle scar on large adult shells. C. cusseta is the terminal Cretaceous member of the C. soleniscus lineage in gulf coast sediments; the lineage continues, however, with little basic modification, throughout the Cenozoic, being represented in the Eocene by C. gigantissima (Finch) and probably, in modern times, by C. virginica (Gmelin). The C. soleniscus lineage is the first typically modern crassostreid group recognized in the Mesozoic.
\nArctostrea aguilerae (Böse) occurs in Late Campanian and Early Maestrichtian sediments of Alabama, Mississippi, Texas(?), Mexico, and Cuba. The mature shell of this species is larger and more massive than that of any other known arctostreid. Arctostrea is well represented throughout the Upper Jurassic and Cretaceous of Europe, but in North America, despite the great numbers and diversity of Cretaceous oysters, only A. aguilerae and the Albian form A. carinata are known. The presence of A. aquilerae in both the Caribbean and gulf coast faunas is exceptional, as the Late Cretaceous faunas of these provinces are generally distinct and originated in different faunal realms.
","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/pp483H","usgsCitation":"Sohl, N.F., and Kauffman, E.G., 1964, Giant Upper Cretaceous oysters from the Gulf coast and Caribbean: U.S. Geological Survey Professional Paper 483, p. H1-H22, https://doi.org/10.3133/pp483H.","productDescription":"p. H1-H22","numberOfPages":"39","costCenters":[],"links":[{"id":117932,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0483h/report-thumb.jpg"},{"id":33838,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0483h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac5e4b07f02db679f3f","contributors":{"authors":[{"text":"Sohl, Norman F.","contributorId":27906,"corporation":false,"usgs":true,"family":"Sohl","given":"Norman","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":152706,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kauffman, Erle G.","contributorId":107756,"corporation":false,"usgs":true,"family":"Kauffman","given":"Erle","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":152707,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1278,"text":"wsp1576E - 1964 - Availability of ground water in parts of the Acoma and Laguna Indian Reservations, New Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1576E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1576","chapter":"E","title":"Availability of ground water in parts of the Acoma and Laguna Indian Reservations, New Mexico","docAbstract":"The need for additional water has increased in recent years on the Acoma and Laguna Indian Reservations in west-central New Mexico because the population and per capita use of water have increased; the tribes also desire water for light industry, for more modern schools, and to increase their irrigation program. Many wells have been drilled in the area, but most have been disappointing because of small yields and poor chemical quality of the water. \r\n\r\nThe topography in the Acoma and Laguna Indian Reservations is controlled primarily by the regional and local dip of alternating beds of sandstone and shale and by the igneous complex of Mount Taylor. The entrenched alluvial valley along the Rio San Jose, which traverses the area, ranges in width from about 0.4 mile to about 2 miles. \r\n\r\nThe climate is characterized by scant rainfall, which occurs mainly in summer, low relative humidity, and large daily fluctuations of temperature. Most of the surface water enters the area through the Rio San Jose. The average annual streamflow past the gaging station Rio San Jose near Grants, N. Mex. is about 4,000 acre-feet. Tributaries to the Rio San Jose within the area probably contribute about 1,000 acre-feet per year. At the present time, most of the surface water is used for irrigation. \r\n\r\nGround water is obtained from consolidated sedimentary rocks that range in age from Triassic to Cretaceous, and from unconsolidated alluvium of Quaternary age. The principal aquifers are the Dakota Sandstone, the Tres Hermanos Sandstone Member of the Mancos Shale, and the alluvium. The Dakota Sandstone yields 5 to 50 gpm (gallons per minute) of water to domestic and stock wells. The Tres Hermanos sandstone Member generally yields 5 to 20 gpm of water to domestic and stock wells. Locally, beds of sandstone in the Chinle and Morrison Formations, the Entrada Sandstone, and the Bluff Sandstone also yield small supplies of water to domestic and stock wells. The alluvium yields from 2 gpm to as much as 150 gpm of water to domestic and stock wells. Thirteen test wells were drilled in a search for usable supplies of ground water for pueblo and irrigation supply and to determine the geologic and hydrologic characteristics of the water-bearing material. The performance of six of the test wells suggests that the sites are favorable for pueblo or irrigation supply wells. The yield of the other seven wells was too small or the quality of the water was too poor for development of pueblo or irrigation supply to be feasible. However, the water from one of the seven wells was good in chemical quality, and the yield was large enough to supply a few homes with water. \r\n\r\nThe tests suggest that the water in the alluvium of the Rio San Jose valley is closely related to the streamflow and that it might be possible to withdraw from the alluvium in summer and replenish it in winter. The surface flow in summer might be decreased by extensive pumpage of ground water, but on the other hand, more of the winter flow could be retained in the area by storage in the ground-water reservoir. Wells could be drilled along the axis of the valley, and the water could be pumped into systems for distribution to irrigated farms. The chemical quality of ground water in the area varies widely from one stratigraphic unit to another and laterally within each unit and commonly the water contains undesirably large amounts of sulfate. However, potable water has been obtained locally from all the aquifers. The water of best quality seemingly is in the Tres Hermanos Sandstone Member of the Mancos Shale and in the alluvium north of the Rio San Jose. The largest quantity of water that is suitable for irrigation is in the valley fill along the Rio San Jose. \r\n\r\nIntensive pumping of ground water from aquifers containing water of good quality may draw water of inferior chemical quality into the wells.","language":"ENGLISH","publisher":"United States Government Printing Office,","doi":"10.3133/wsp1576E","usgsCitation":"Dinwiddie, G.A., and Motts, W.S., 1964, Availability of ground water in parts of the Acoma and Laguna Indian Reservations, New Mexico: U.S. Geological Survey Water Supply Paper 1576, iv, 65 p. :ill., map ;24 cm. & 3 maps in pocket., https://doi.org/10.3133/wsp1576E.","productDescription":"iv, 65 p. :ill., map ;24 cm. & 3 maps in pocket.","costCenters":[],"links":[{"id":137528,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1576e/report-thumb.jpg"},{"id":26238,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1576e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26239,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1576e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26240,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1576e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26241,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1576e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65db99","contributors":{"authors":[{"text":"Dinwiddie, George A.","contributorId":21135,"corporation":false,"usgs":true,"family":"Dinwiddie","given":"George","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":143488,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Motts, Ward Sundt","contributorId":68708,"corporation":false,"usgs":true,"family":"Motts","given":"Ward","email":"","middleInitial":"Sundt","affiliations":[],"preferred":false,"id":143489,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1947,"text":"wsp1748 - 1964 - Apparatus and techniques for measuring bedload","interactions":[],"lastModifiedDate":"2012-02-02T00:05:22","indexId":"wsp1748","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1748","title":"Apparatus and techniques for measuring bedload","docAbstract":"The need for accurate determinations of the total sediment discharge of particles of bedload size has prompted this investigation of available and possible measuring apparatus and procedures. The accuracy of measurements of sediment discharge made with trap-type samplers is affected by the variability of sampler efficiency, by the oscillatory variation of bedload discharge, and by sampler placement. Equations that were developed for determining total discharge from measured bedioad discharge and measured suspended-sediment discharge are simplest if the bedload apparatus measures only the true bedload. \r\n\r\nEarly bedload samplers are generally unsatisfactory. Recently developed or suggested apparatus include various improved samplers of the pressure-difference type, a pumping sampler, a magnetic sampler, acoustical instruments that measure the magnitude of the sound of particle collisions, an ultrasonic bedload sampler designed to measure and integrate electronically the concentration and velocity, and a tiltmeter designed to measure the total sediment discharge from the ground tilt that results from the passage of flow. All the pressure-difference samplers are improvements over early samplers, but none are void of the inherent shortcomings of trap-type apparatus; probably the Sphinx (Dutch) and VUV (Hungarian) samplers are the most satisfactory. The acoustical instruments are capable of measuring only the relative discharge. The ultrasonic sampler and the tiltmeter are not adequate without further development. \r\n\r\nSome new possible apparatus and means for measuring or aiding in measuring bedload discharge are small pit samplers, ultrasonic sounders, pressure transducers, and photography. A small pit sampler for measuring bedload discharge was designed to provide self-placement and portability ; however, its practicability and efficiency are undetermined. Exploratory films show that by using slowmotion photography the discharge of particles larger than about pea size can be determined provided the flow is clear; however, photography generally is not practical. Ultrasonic sounders provide continuous and accurate data on bed configuration and dune movement for use in equations that were developed for computing the bedload discharge. Computations with the equations indicate that the interpretation of the sounding data needs further study. Pressure transducers placed beneath the bed surface possibly can be used to provide information on dune movement; however, their installation would be difficult. The time required for collecting data on bed configuration and dune movement throughout a cross section could be substantially reduced by using several transducers simultaneously in conjunction with an ultrasonic sounder. A modified ultrasonic sounder that provides information on the shape and velocity of large particles and a method for determining the discharge of such particles were proposed; the method seems most feasible for particles of high sphericity.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1748","usgsCitation":"Hubbell, D.W., 1964, Apparatus and techniques for measuring bedload: U.S. Geological Survey Water Supply Paper 1748, v, 74 p. :illus. ;24 cm., https://doi.org/10.3133/wsp1748.","productDescription":"v, 74 p. :illus. ;24 cm.","costCenters":[],"links":[{"id":27278,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1748/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138418,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1748/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4883e4b07f02db51824d","contributors":{"authors":[{"text":"Hubbell, David Wellington","contributorId":88330,"corporation":false,"usgs":true,"family":"Hubbell","given":"David","email":"","middleInitial":"Wellington","affiliations":[],"preferred":false,"id":144417,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2253,"text":"wsp1777 - 1964 - Geology and ground-water resources of Washington County, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1777","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1777","title":"Geology and ground-water resources of Washington County, Colorado","docAbstract":"Washington County, in northeastern Colorado, has an area of 2,520 square miles. The eastern two-thirds of the county, part of the High Plains physiographic section, is relatively flat and has been moderately altered by the deposition of loess and dune sand, and by stream erosion. The western one-third is a part of the South Platte River basin and has been deeply dissected by tributary streams. The soils and climate of the county are generally suited for agriculture, which is the principal industry. \r\n\r\nThe rocks that crop out in the county influence the availability of ground water. The Pierre Shale, of Late Cretaceous age, underlies the entire area and ranges in thickness from 2,000 to 4,500 feet. This dense shale is a barrier to the downward movement of water and yields little or no water to wells. The Chadron Formation, of Oligocene age, overlies the Pierre Shale in the northern and central parts of the area. The thickness of the formation ranges from a few feet to about 300 feet. Small to moderate quantities of water are available from the scattered sand lenses and from the highly fractured zones of the siltstone. The Ogallala Formation, of Pliocene age, overlies the Chadron Formation and in Washington County forms the High Plains section of the Great Plains province. The thickness of the Ogallala Formation ranges from 0 to about 400 feet, and the yield from wells ranges from a few gallons per hour to about 1,500 gpm. Peorian loess, of Pleistocene age, and dune sand, of Pleistocene to Recent age, mantle a large pan of the county and range in thickness from a few inches to about 120 feet Although the loess and dune sand yield little water to wells, they absorb much of the precipitation and conduct the water to underlying formations. Alluvium, of Pleistocene and Recent age, occupies most of the major stream valleys in thicknesses of a few feet to about 250 feet. The yield of wells tapping the alluvium ranges from a few gallons per minute to about 3,000 gpm, according to the thickness of saturated material. \r\n\r\nDevelopment of ground water for irrigation has been generally restricted to the South Platte, Arikaree, and Beaver valleys. There were 134 irrigation wells, 3 industrial wells, and 10 municipal wells in the county in 1959. The annual ground-water pumpage from Washington County is estimated to be 18,000 acre-ft; about 10,000 acre-ft is from the High Plains ground-water province. Although some ground water enters the county as underflow, most of the recharge to ground-water reservoirs is from precipitation on the land surface. Recharge to the Ogallala Formation in the county is assumed to be approximately equal to the natural discharge from the county by underflow because ground-water withdrawals are from storage, and no other significant amount of natural discharge is apparent. Undertow in the Ogallala was calculated to be 83,000 acre-ft per year and the rate of recharge from precipitation to be about 0.95 inch per year. Neither recharge nor discharge was calculated for that part of the county in the South Platte River basin. \r\n\r\nAll ground water in Washington County has a high proportion of carbonate and is classed as hard to very hard. The sodium-adsorption-ratio for all samples analyzed was below the limit recommended for irrigation water. All the water from the Ogallala Formation and most of the water from the Chadron Formation is suitable for domestic use. Some water from the alluvial deposits overlying the Pierre Shale was exceptionally high in calcium, magnesium, and sodium sulfates. \r\n\r\nGround water has been heavily developed for irrigation in the South Platte valley and in some parts of the Beaver and Arikaree valleys. Some additional areas, however, could be developed in the latter two valleys. Large quantities of ground water in the Ogallala Formation are available for future development. The quantity of water in storage in the High Plains ground-water province in Washington County is about 6.5 million acre-f","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1777","usgsCitation":"McGovern, H.E., 1964, Geology and ground-water resources of Washington County, Colorado: U.S. Geological Survey Water Supply Paper 1777, iv, 46 p. :illus., maps (4 fold. 1 col., in pocket) ;24 cm., https://doi.org/10.3133/wsp1777.","productDescription":"iv, 46 p. :illus., maps (4 fold. 1 col., in pocket) ;24 cm.","costCenters":[],"links":[{"id":110015,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24953.htm","linkFileType":{"id":5,"text":"html"},"description":"24953"},{"id":137835,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1777/report-thumb.jpg"},{"id":28024,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28025,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28026,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28027,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1777/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28028,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1777/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68580b","contributors":{"authors":[{"text":"McGovern, Harold E.","contributorId":9634,"corporation":false,"usgs":true,"family":"McGovern","given":"Harold","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144901,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1296,"text":"wsp1812 - 1964 - Public water supplies of the 100 largest cities of the United States, 1962","interactions":[],"lastModifiedDate":"2017-09-06T17:56:12","indexId":"wsp1812","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1812","title":"Public water supplies of the 100 largest cities of the United States, 1962","docAbstract":"The public water supplies of the 100 largest cities in the United States (1960 U.S. Census) serve 9,650 million gallons of water per day (mgd) to 60 million people, which is 34 percent of the Nation's total population and 48 percent of the Nation's urban population. The amount of water used to satisfy the domestic needs as well as the needs of commerce and industry ranges from 13 mgd, which serves a population of 124,000, to 1,200 mgd, which serves a city of 8 million people.
\nThe water for the public supplies of these largest cities comes fro^n ground water wells and infiltration galleries and from surface water streams, reservoirs, and lakes. Twenty of the cities use ground water exclusively for public supplies, and 14 use a combination of ground and surface waters. Sixty-six cities use surface water solely; of these cities 37 depend solely upon reservoir water, and 20 depend solely upon natural streamflow. Water from the Great Lakes furnishes part or all of the water supply for 10 of these largest cities.
\nHardness of water, measured in parts per million (ppm), is an important factor in the usability of water supplies. Twenty-seven cities, serving a population of 8 million, have a raw-water hardness exceeding 180 ppm (\"very hard\"), but only 13 cities, serving a population of 3.7 million, have a \"very hard\" treated-water supply; and although 22 cities, serving about 10 million people, have a raw-water hardness ranging from 121 to 180 ppm (\"hard\"), only 16 cities, serving a population of 11 million, have a \"hard\" treated-water supply. Only 16 cities, serving a population of 16 million people, have a raw-water hardness ranging from 61 to 120 ppm (\"moderately hard\"), whereas 41 cities, serving a population of 22 million, have a treated-water supply having a hardness within this desirable range. A few cities that have a \"soft\" raw water add lime to control corrosion and consequently increase their water hardness to more than 61 ppm. Thirty cities, serving a population of about 23 million, have a treated-water supply with a hardness of less than 61 ppm.
\nThe dissolved-solids content in raw-water supplies of 27 cities, which serve a total population of slightly more than 21 million people, is 100 ppr^ or less. Thirty-eight cities serving a total population of 23 million people have raw-water supplies with a dissolved-solids content between 101 and 250 ppm, whereas 48 cities, serving a population of 28 million about half the population of these 1 2 PUBLIC WATER SUPPLIES, 1962 cities furnish water having this range of dissolved solids. Twentv-nine cities serving a total population of 11 million people have raw-water supplies that contain between 251 to 500 ppm of dissolved solids. Because some o* these cities treat their water supply, 22 cities serving 8 million people furnish water having a dissolved-solids content between 251 and 500 ppm. Only six cities, serving a population of about iy2 million people, have raw-water supplies containing more than 500 ppm of dissolved solids; four of these cities soften the water and consequently reduce the dissolved-solids content. Thus, about 1 million people in three cities receive water containing more than 500 ppm of dissolved solids.
\nChemical analyses of treated-water supplies indicate that more than 90 percent of the supplies contain less than (a) 500 ppm of dissolved solids, (b) 100 ppm of sulfate, (c) 50 ppm each of calcium, sodium, and chloride, (d) 30 ppm of silica, (e) 20 ppm of magnesium, (f) 5 ppm each of potassium and nitrate, and (g) 1 ppm of fluoride.
\nSpectrographic analyses, reported in micrograms per liter (/*g per 1), show that 87 percent of the treated-water supplies contain less than 500 /*g per 1 of aluminum and more than 90 percent of the supplies contain less than (a) 500 /*g per 1 of strontium, (b) 150 /*g per 1 of iron, (c) 50 ^g per 1 of lithium, (d) 10 /ug per 1 each of molybdenum, nickel, lead, and vanadium, and (e) 5 /*g per 1 each cf chromium, rubidium, and titanium.
\nRadiochemical analyses of treated-water supplies reveal that the maximum beta activity of these supplies is 130 picocuries per liter (pc per 1) and the maximum activity due to radium content is 2.5 pe per 1, both of which are well under the recommended maximum limits for drinking water.
\nThe report is divided into two sections. The first describes the uses of water in large cities, the raw-water supplies available for public supplies, tl-<; major and minor constituents and the properties of water, the methods of analyses, the treatment of water, the effects of chemical treatment on constituents and properties of water, and the costs of water treatment. The second is a city-by-city inventory that gives (a) the population of the city, (b) the adjacent communities supplied by the city water system, (c) the total population served, (d) the sources of water supply (including auxiliary and emergency supplies), (e) the average amount of water used daily, (f) the lowest 30-day mean discharge of streams used for public supply during recent years, (g) the treatment of water, (h) the rated capacity of each water-treatment plant, and (i) the storage capacity for raw and finished water. For 58 of the cities, the sources of water, the location of water-treatment plants, and the areas served by the city system are shown on maps. Chemical, spectrographic, and radiochemical analyses of treated water and chemical and spectrographic analyses for many of the raw-water supplies are presented in tabular form.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington,D.C.","doi":"10.3133/wsp1812","usgsCitation":"Durfor, C.N., and Becker, E., 1964, Public water supplies of the 100 largest cities of the United States, 1962: U.S. Geological Survey Water Supply Paper 1812, ix, 364 p., https://doi.org/10.3133/wsp1812.","productDescription":"ix, 364 p.","numberOfPages":"372","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true},{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true},{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":26290,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1812/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137036,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1812/report-thumb.jpg"}],"country":"United 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States\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a90e4b07f02db65611a","contributors":{"authors":[{"text":"Durfor, Charles N.","contributorId":50881,"corporation":false,"usgs":true,"family":"Durfor","given":"Charles","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":143519,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Becker, Edith","contributorId":10401,"corporation":false,"usgs":true,"family":"Becker","given":"Edith","email":"","affiliations":[],"preferred":false,"id":143518,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1233,"text":"wsp1499H - 1964 - Water resources of the Hartford-New Britain area, Connecticut","interactions":[],"lastModifiedDate":"2022-12-19T21:17:22.931346","indexId":"wsp1499H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1499","chapter":"H","title":"Water resources of the Hartford-New Britain area, Connecticut","docAbstract":"The Hartford-New Britain area includes the metropolitan areas of Hartford and New Britain and parts of several adjoining towns. Water used in the area is withdrawn from the principal streams and aquifers at an average rate of 463.5 mgd (million gallons per day). Sufficient water is available from these sources to meet present requirements and those for many years to come, although local shortages may develop in some areas as the result of problems of distribution and treatment. About 98 percent of all water used in 1957 was from surface sources. More than 425 mgd was required by industry, and about 23 mgd was for domestic water supply. The Farmington River upstream from Collinsville is the chief source of water for public supply in the Hartford-New Britain area, whereas the Connecticut River is the chief source of water for industry. An average of about 40 mgd is withdrawn from the upper Farmington River for public supply, and about 404 mgd is withdrawn by industry from the Connecticut River for nonconsumptive use and returned directly to the stream.
The Connecticut River is the source of the largest quantity of water in the area. The flow of the stream at Thompsonville may be expected to equal or exceed about 2,000 mgd 95 percent of the time, and the flow should not be less than this amount for periods longer than 12 days. The flow below Thompsonville is increased by additions from the Scantic, Farmington, Park, and Hockanum Rivers and from numerous smaller tributary streams. The available streamflow data for the aforementioned rivers have been summarized graphically in the report.
The chemical quality of water in the Connecticut River is good, except for short periods when the iron concentration is high. In addition to the removal of iron some other treatment may be necessary if water from the Connecticut River is used for special purposes. The chemical quality of the tributary streams is good, except the quality of the Park River, which is poor. Thus the Connecticut River in the vicinity of Hartford offers an almost unlimited source of water of good chemical quality to the Hartford, New Britain area. The Connecticut River and many of its tributaries, however, are polluted to some degree, and the cost of treatment for pollution and of delivery of water to the area presents an economic problem in the further development of these sources.
The Hartford-New Britain area in the vicinity of Hartford has been plagued by floods since the time of its settlement. Most of the damage to property and loss of life in the Hartford area has been caused by flooding of the Connecticut and Park Rivers. Floods have occurred on the Connecticut River and its tributaries in every month of the year, but the most severe floods occur in the spring and fall. The most devastating flood on the Connecticut River occurred on March 21, 1986, when the stage at Hartford reached 37.0 feet above mean sea level. The maximum flood on the Park River occurred on August 19, 1955, when the stage reached 43.5 feet above mean sea level. Floods on the other tributaries have been frequent and some have been large, but damage has not been as great because the streams flow mostly through rural areas.
Small to moderate supplies of water suitable for domestic use and for small municipalities and industries are available from wells in the Hartford-New Britain area. Moderate supplies are obtainable from five definable sand-and-gravel aquifers and from widespread consolidated sedimentary rocks. Yields to individual wells range from 15 to 400 gpm (gallons per minute) for wells penetrating sand and gravel and from 1 to 578 gpm for wells penetrating consolidated sedimentary rocks. Sand and gravel deposits bordering the Connecticut River downstream from Rocky Hill afford the greatest potential for the development of large supplies of ground water. Small supplies ranging from 1 to 40 gpm are obtainable from glacial till and from consolidated crystalline rocks.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1499H","usgsCitation":"Cushman, R.V., Tanski, D., and Thomas, M.P., 1964, Water resources of the Hartford-New Britain area, Connecticut: U.S. Geological Survey Water Supply Paper 1499, Report: vi, 96 p.; 2 Plates: 24.00 × 27.53 inches and 24.50 × 31.32 inches, https://doi.org/10.3133/wsp1499H.","productDescription":"Report: vi, 96 p.; 2 Plates: 24.00 × 27.53 inches and 24.50 × 31.32 inches","costCenters":[],"links":[{"id":138071,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499h/report-thumb.jpg"},{"id":26160,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499h/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26158,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499h/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26159,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499h/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":410735,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24444.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Connecticut","city":"Hartford, New Britain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -72.5670,\n 41.875\n ],\n [\n -72.875,\n 41.875\n ],\n [\n -72.875,\n 41.625\n ],\n [\n -72.5670,\n 41.625\n ],\n [\n -72.5670,\n 41.875\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49efe4b07f02db5eda7b","contributors":{"authors":[{"text":"Cushman, Robert Vittum","contributorId":96661,"corporation":false,"usgs":true,"family":"Cushman","given":"Robert","email":"","middleInitial":"Vittum","affiliations":[],"preferred":false,"id":143414,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tanski, D.","contributorId":83385,"corporation":false,"usgs":true,"family":"Tanski","given":"D.","email":"","affiliations":[],"preferred":false,"id":143413,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, M. P.","contributorId":62574,"corporation":false,"usgs":true,"family":"Thomas","given":"M.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":143412,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":975,"text":"wsp1653 - 1964 - Ground-water resources of the lower Rio Grande Valley area, Texas","interactions":[],"lastModifiedDate":"2016-08-22T11:21:21","indexId":"wsp1653","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1653","title":"Ground-water resources of the lower Rio Grande Valley area, Texas","docAbstract":"The report contains information about the occurrence, quality, and use of ground water in the Lower Rio Grande Valley area which consists of Cameron, Hidalgo, Starr, and Willacy Counties in southern Texas.
\nThe principal use of water in the area is for irrigation. The principal irrigated crops are cotton, winter vegetables, and citrus fruits. In southeastern Starr County, southern Hidalgo County, and western Cameron County, the main source of water is the Rio Grande. The greatest development of ground water in this area was after 1948 when ground water was needed to supplement water from the river.
\nThe Lower Rio Grande Valley area has four major ground-water reservoirs. Because of the uncertainty in mapping the stratigraphic units and because some of the ground-water reservoirs are composed of parts of two or more formations, three of the ground-water reservoirs have been given names in this report. The major ground-water reservoirs are: the Oakville sandstone, an important source of water for industrial use in northeastern Stair County; the Linn-Faysville ground-water reservoir, which supplies irrigation water in the Linn-Faysville area in central Hidalgo County; and the Rio Grande ground-water reservoir and the Mercedes-Sebastian shallow ground-water reservoir, both of which supply considerable irrigation water in southeastern Starr, southern Hidalgo, western Cameron, and southwestern Willacy Counties.
\nThe quality of water differs considerably from place to place in the Lower Rio Grande Valley area. In most of the area, water is available that can be used for domestic or public supply, but it generally is slightly saline. In most of the area, the ground water is unsuitable for irrigation .particularly if used exclusively. Water of the best quality in the area is from the Rio Grande groundwater reservoir near the Rio Grande at depths of less than 75 feet in southeastern Stair County, between 50 and 250 feet in southern Hidalgo County, and between 100 and 300 feet in western Cameron County. At progressively greater distances from the Rio Grande, the ground water at these depths tends to be more mineralized. Also at some places at depths greater than those indicated, the water tends to be more mineralized. In the Linn-Faysville area the ground water from the Linn-Faysville ground-water reservoir is moderately mineralized and ranges from fair to unsuitable for irrigation.
\nIn western Cameron County, water levels in some wells tapping the Rio Grande ground-water reservoir declined about 10 feet from 1954 to 1957. In 1959 the water levels stood higher than in 1954. The water levels in most wells tapping the Linn-Faysville ground-water reservoir declined 10 feet or more from 1948 to 1958. In some wells the decline was more than 15 feet.
\nThe available information indicates that in some localities the Rio Grande ground-water reservoir may be nearly filled to capacity, and waterlogging will occur during periods of above-normal precipitation. During protracted periods of below-normal precipitation, the available water in the ground-water reservoir may be depleted.
\nFurther studies should be made in the area to correct important deficiencies in available information. A continuing program is recommended because information such as fluctuations in water levels and the amount and distribution of pumping can be obtained only on a current basis.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1653","usgsCitation":"Baker, R.C., and Dale, O., 1964, Ground-water resources of the lower Rio Grande Valley area, Texas: U.S. Geological Survey Water Supply Paper 1653, Report: v, 56 p.; 5 Plates, https://doi.org/10.3133/wsp1653.","productDescription":"Report: v, 56 p.; 5 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":25537,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1653/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137059,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1653/report-thumb.jpg"},{"id":25532,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25533,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25534,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25535,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25536,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1653/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cde4b07f02db54492c","contributors":{"authors":[{"text":"Baker, R. C.","contributorId":79084,"corporation":false,"usgs":true,"family":"Baker","given":"R.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":142951,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dale, O.C.","contributorId":28583,"corporation":false,"usgs":true,"family":"Dale","given":"O.C.","email":"","affiliations":[],"preferred":false,"id":142950,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2046,"text":"wsp1499G - 1964 - Water resources of the Green Bay area, Wisconsin","interactions":[],"lastModifiedDate":"2021-08-16T21:39:30.070959","indexId":"wsp1499G","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1499","chapter":"G","title":"Water resources of the Green Bay area, Wisconsin","docAbstract":"The Green Bay area comprises an area of about 525 square miles in eastern Wisconsin at the south end of Green Bay. It includes the western three-fourths of Brown County and the eastern one-ninth of Outagamie County. In 1960, the population of the area was estimated at 124,000.
\nThe most prominent topographic feature is the northwest-facing, southwestward trending Niagara escarpment. The area northwest of the escarpment drains into Green Bay via the Fox River, Suamico River, Duck Creek, and their tributaries. The area southeast of the escarpment is drained by streams that flow into Lake Michigan.
\nThe chief sources of surface water in the Green Bay area are the Fox River, Green Bay, and Lake Michigan. Smaller amounts of water are available from the East and Suamico Rivers and other streams. A sandstone aquifer is the principal source of the ground-water supply. The Niagara dolomite, although largely undeveloped, is potentially an important aquifer in the eastern part of the area. Small amounts of water are obtained also from the Platteville formation and from deposits of Pleistocene and Recent age. Water from the surfaceand ground-water sources is moderately hard to very hard.
\nThe Fox River, tributary to Lake Michigan at Green Bay, is a significant source of water for industrial use in the Green Bay area. The Menasha Dam, which controls release of water from the Lake Winnebago pool, is the major regulation on the Fox River, and it has considerable effect in reducing peak flows and supplementing low flows in the lower Fox River. The average discharge of the lower Fox River for the period 1898-1959, as measured at the gaging station at Rapide Croche Dam, was 2,687 mgd (million gallons per day). The longest consecutive period during which the discharge averaged less than 500 mgd was 80 days. The average discharge can be expected to fall below 700 mgd about once every 5 years for a 7-day period. In 1959, the average withdrawal of water from the Fox River was about 62 mgd. The water in the river is of the calcium magnesium bicarbonate type and is hard.
\nThe small streams in the area are utilized chiefly for stock watering; some of the water, however, is used for irrigation. The water in the small streams is more highly mineralized than the water in the Fox River and is very hard.
\nLarge quantities of water are available from Green Bay, but the disposal of industrial waste into the bay has restricted the use of the water. The major withdrawal is for condenser cooling, and, in 1959, it averaged about 415 mgd. The water from Green Bay is moderately hard but is of better chemical quality than the water from the Fox River and the small streams in the area.
\nThe only withdrawals of water from Lake Michigan for use in the Green Bay area are made by the city of Green Bay. In 1959, these withdrawals averaged 7.8 mgd.
\nThe lower Fox River is not subject to extremes of flow owing to the dampening effect of the Lake Winnebago pool and the regulation of flow at Menasha Dam. Cloudbursts over the lower Fox River valley below Menasha Dam, however, have occasionally caused extremely high water, as in 1922, when the discharge at the mouth of the Fox River was estimated to be about 50,000 mgd. Daily discharges greater than about 13,000 mgd occurred only 7 times in the period 1918-59. The 50-year flood of 15,500 mgd represents an average runoff of less than 2.6 mgd per square mile of drainage area, a relatively low runoff for a 50-year flood in Wisconsin.
\nThe sandstone aquifer is the principal source of ground water in the Green Bay area and furnishes water for public supply and industrial use. This aquifer includes rocks of Late Cambrian age, and the Prairie du Chien group and St. Peter sandstone of Ordovician age; it ranges in thickness from 550 to 640 feet. Ground water is found in openings along fractures and bedding planes and in the interstices between sand grains.
\nThe sandstone aquifer can support additional development of large supplies of ground water. Wells can be developed in most of the area that will yield 500 gpm (gallons per minute) or more, provided they are properly spaced and penetrate the entire thickness of the aquifer. It is estimated that the perennial yield of the sandstone in the Green Bay area could be at least 30 mgd if the aquifer is properly developed; only 5.4 mgd was withdrawn in 1959. The water from this sandstone aquifer is of the calcium magnesium bicarbonate type, is very hard, and, at a few places, contains objectionable amounts of iron.
\nThe Niagara dolomite, potentially a source of moderate to large quantities of water in the eastern part of the area, probably will yield 500 gpm or more to wells.
\nIn 1959, the average withdrawal of water for all uses was estimated at 495 mgd, of which 98.2 percent was from surface-water sources and 1.8 percent was from wells. About 485 mgd of water was withdrawn for industrial use, 6 mgd for public supply, and 4 mgd for rural use. The industrial use of water averaged 441 mgd for condenser cooling, 38 mgd fot processing by the paper industry, and 6 mgd for other industrial uses. The city of Green Bay used 7.8 mgd of water from Lake Michigan; other public supplies in the area used 2.6 mgd from wells. Of the withdrawals of water for rural use, about 75 percent was from wells and about 25 percent was from streams.
\nThe discharge of wastes into the lower Fox River and its tributary streams has altered the quality of the natural water. The wastes consist chiefly of treated municipal sewage and treated and untreated wastes from the paper industry, rendering plants, a sugar mill, and other industries. The industrial waste makes up about 90 percent of the oxygen-demand loading in the lower Fox River, and treated municipal sewage accounts for about 10 percent. The dissolved-oxygen concentration of water in the lower Fox River decreases rapidly in the vicinity of Green Bay during the summer when the river water is warm. If the periods when the river water is warmest, generally during July and early August, were to coincide with periods of lowest annual streamflow, generally in late August, the river would be unable to assimilate the loading of decomposable organic matter.
\nIn an emergency, industrial and public supply wells could supply at least 6 mgd for a sustained period and probably as much as 10 mgd for a period of several days. Six of the wells that formerly supplied the city of Green Bay are maintained in operating condition and could furnish about the same quantity of water as the industrial and other public supply wells. Small streams in the area would be supplemental sources of water, and the water in the Fox River and Green Bay is easily accessible.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Water resources of industrial regions: A summary of the source, occurrence, availability, and use of water in the area","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1499G","usgsCitation":"Knowles, D.B., Dreher, F.C., and Whetstone, G.W., 1964, Water resources of the Green Bay area, Wisconsin: U.S. Geological Survey Water Supply Paper 1499, Report: v, 67 p.; 1 Plate: 23.50 x 31.95 inches, https://doi.org/10.3133/wsp1499G.","productDescription":"Report: v, 67 p.; 1 Plate: 23.50 x 31.95 inches","numberOfPages":"78","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":27567,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499g/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27568,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499g/report.pdf"},{"id":387952,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24443.htm"},{"id":137727,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499g/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Brown County, Oconto County, Outagamie County","city":"Green Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.25,\n 44.25\n ],\n [\n -88.25,\n 44.6670\n ],\n [\n -87.90,\n 44.6670\n ],\n [\n -87.90,\n 44.25\n ],\n [\n -88.25,\n 44.25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db634ad6","contributors":{"authors":[{"text":"Knowles, Doyle Blewer","contributorId":9633,"corporation":false,"usgs":true,"family":"Knowles","given":"Doyle","email":"","middleInitial":"Blewer","affiliations":[],"preferred":false,"id":144585,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dreher, F. C.","contributorId":93878,"corporation":false,"usgs":true,"family":"Dreher","given":"F.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144587,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Whetstone, George Walter","contributorId":30603,"corporation":false,"usgs":true,"family":"Whetstone","given":"George","email":"","middleInitial":"Walter","affiliations":[],"preferred":false,"id":144586,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1283,"text":"wsp1757B - 1964 - Ground-water resources of the Bengasi area, Cyrenaica, United Kingdom of Libya","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1757B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1757","chapter":"B","title":"Ground-water resources of the Bengasi area, Cyrenaica, United Kingdom of Libya","docAbstract":"The Benpsi area of Libya, in the northwestern part of the Province of Cyrenaica (Wilayat Barqah), is semiarid, and available ground-water supplies in the area are relatively small. Potable ground water from known sources is reserved for the present and future needs of the city, and no surface-water supplies are available in the area. This investigation to evaluate known, as well as potential, water supplies in the area was undertaken as part of a larger program of ground-water investigations in Libya under the auspices of the U. S. Operations Mission to Libya and the Government of Libya. \r\n\r\nA ground-water reservoir underlies the Bengasi area, in which the water occurs in solution channels, cavities, and other openings in Miocene limestone. The reservoir is recharged directly by rainfall on the area and by infiltration from ephemeral streams (wadis) rising in Al Jabal al Akhar to the east. In the Baninah and Al Fuwayhit areas the ground-water reservoir yields water of fair quality and in sufficient quantity for the current (1959) needs. of the Bengasi city supply. The test-drilling program in the area south and southeast of Bengasi indicates that water in sufficient quantity for additional public supply probably can be obtained in some localities from wells. The water, however, is moderately to highly mineralized and would require treatment or demineralization before it could be used for additional public supply. Much of the water could be used directly for irrigation, but careful attention would have to be given to cultivation, drainage, and cropping practices. The hazard of saltwater encroachment also exists if large-scale withdrawals are undertaken in the coastal zones.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1757B","usgsCitation":"Doyel, W.W., and Maguire, F.J., 1964, Ground-water resources of the Bengasi area, Cyrenaica, United Kingdom of Libya: U.S. Geological Survey Water Supply Paper 1757, iii, 21 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1757B.","productDescription":"iii, 21 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137246,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757b/report-thumb.jpg"},{"id":26246,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d462","contributors":{"authors":[{"text":"Doyel, William Watson","contributorId":74355,"corporation":false,"usgs":true,"family":"Doyel","given":"William","email":"","middleInitial":"Watson","affiliations":[],"preferred":false,"id":143498,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Maguire, Frank J.","contributorId":66662,"corporation":false,"usgs":true,"family":"Maguire","given":"Frank","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143497,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2203,"text":"wsp1764 - 1964 - Ground-water geology of the Dickson, Lawrenceburg, and Waverly areas in the western Highland Rim, Tennessee","interactions":[],"lastModifiedDate":"2024-01-31T20:36:24.280058","indexId":"wsp1764","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1764","title":"Ground-water geology of the Dickson, Lawrenceburg, and Waverly areas in the western Highland Rim, Tennessee","docAbstract":"Ground-water supplies in the Dickson, Lawrenceburg, and Waverly areas are obtained from wells and springs in limestone and chert formations of Missisippian age. In the Dickson area most of the wells and springs are in Warsaw Limestone. In the Lawrenceburg and Waverly areas, ground-water supplies are obtained from Fort Payne Chert and from residuum. In all three areas a few wells obtain small amounts of water from gravel stringers in the residuum. \r\n\r\nYields of well range from a few to 300 gpm (gallons per minute). Wells having the largest yields obtain water from residual material (colluvium) in the valley of Trace Creek in the Waverly area. Fewer than 10 percent of all wells inventoried yield more than 25 gpm. Springs are common in all the areas studied and yield as much as 1,000 gpm. \r\n\r\nThe quality of water from wells and springs iv the areas studied generally is good. The water is of the calcium bicarbonate type, and most of it is moderately hard to hard. The constituents in water from springs and from wells are about the same, although water from springs tends to be softer and slightly lower in dissolved-solids content. \r\n\r\nSprings constitute the largest potential source of water in the three areas. Twenty-one of the large springs discharge approximately 12 million gallons per day, or about 8,000 gpm. Another potential source of water is residuum underlying the valley of Trace Creek in the Waverly area. Wells yielding as much as 500 gpm probably could be developed in this aquifer.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1764","usgsCitation":"Marcher, M.V., Bingham, R.H., and Lounsbury, R., 1964, Ground-water geology of the Dickson, Lawrenceburg, and Waverly areas in the western Highland Rim, Tennessee: U.S. Geological Survey Water Supply Paper 1764, Report: iv, 50 p.; 7 Plates: 19.68 × 38.83 inches or smaller, https://doi.org/10.3133/wsp1764.","productDescription":"Report: iv, 50 p.; 7 Plates: 19.68 × 38.83 inches or smaller","costCenters":[],"links":[{"id":27871,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397419,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24942.htm","text":"Lawrenceburg area"},{"id":27866,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27867,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27868,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138156,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1764/report-thumb.jpg"},{"id":27865,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27869,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27870,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1764/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27872,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1764/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397418,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24941.htm","text":"Dickson area"},{"id":397420,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24943.htm","text":"Waverly area"}],"scale":"31680","country":"United States","state":"Tennessee","city":"Dickson, Lawrenceburg, Waverly","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.5,\n 36\n ],\n [\n -87.25,\n 36\n ],\n [\n -87.25,\n 36.125\n ],\n [\n -87.5,\n 36.125\n ],\n [\n -87.5,\n 36\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.375,\n 35.125\n ],\n [\n -87.25,\n 35.125\n ],\n [\n -87.25,\n 35.375\n ],\n [\n -87.375,\n 35.375\n ],\n [\n -87.375,\n 35.125\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.875,\n 36\n ],\n [\n -87.75,\n 36\n ],\n [\n -87.75,\n 36.125\n ],\n [\n -87.875,\n 36.125\n ],\n [\n -87.875,\n 36\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d966","contributors":{"authors":[{"text":"Marcher, Melvin V.","contributorId":11590,"corporation":false,"usgs":true,"family":"Marcher","given":"Melvin","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":144819,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bingham, Roy H.","contributorId":56632,"corporation":false,"usgs":true,"family":"Bingham","given":"Roy","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144820,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lounsbury, Richard Edwin","contributorId":102054,"corporation":false,"usgs":true,"family":"Lounsbury","given":"Richard Edwin","affiliations":[],"preferred":false,"id":144821,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1054,"text":"wsp1695 - 1964 - Geology and ground-water resources of southeastern New Hampshire","interactions":[{"subject":{"id":51806,"text":"ofr5516 - 1955 - Preliminary report on the investigation of ground-water resources of the seacoast region of New Hampshire","indexId":"ofr5516","publicationYear":"1955","noYear":false,"title":"Preliminary report on the investigation of ground-water resources of the seacoast region of New Hampshire"},"predicate":"SUPERSEDED_BY","object":{"id":1054,"text":"wsp1695 - 1964 - Geology and ground-water resources of southeastern New Hampshire","indexId":"wsp1695","publicationYear":"1964","noYear":false,"title":"Geology and ground-water resources of southeastern New Hampshire"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1695","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1695","title":"Geology and ground-water resources of southeastern New Hampshire","docAbstract":"The continued growth and development of southeastern New Hampshire, an area of about 390 square miles adjacent to the Atlantic Ocean, will depend partly on effectively satisfying the demand for water, which has increased rapidly since World War II. \r\n\r\nThe report identifies and describes the principal geologic units with respect to the occurrence of ground water. These units include bedrock and the various unconsolidated deposits that mantle the bedrock surface discontinuously throughout the area. \r\n\r\nThe bedrock formations, consisting of igneous and metamorphic rocks, chiefly of Paleozoic age, form a single water-bearing unit. Ground water is in joints and fractures. The fractures are small and scattered and therefore impart only a low permeability to the rocks. Wells in the bedrock commonly produce small but reliable supplies of ground water at depths of less than 150 feet. The yields of about 80 wells inventoried for this report ranged from 1? to 100 gpm (gallons per minute) and the median was 912 gpm. Depths ranged from 45 to 600 feet. The unconsolidated deposits consist of glacial drift of Pleistocene age; swamp deposits, alluvium, and beach deposits of Recent age; and eolian deposits of Pleistocene -and Recent age. For this report the glacial drift is divided into till, ice-contact deposits, marine deposits, and outwash and shore deposits. Glacial till forms a discontinuous blanket, commonly less than 15 but in some hills (drumlins) as much as about 200 feet thick. It has a low permeability but, because of its widespread outcrop area, it has been utilized as a source of water for numerous domestic supplies. Because most wells in till are shallow, many fail to meet modern demands during dry summers. \r\n\r\nIce-contact deposits locally form kames, kame terraces, kame plains, and ice-channel fillings throughout the area. They overlie bedrock and till and range in thickness from less than 1 foot to as much as 190 feet. In general, the ice-contact deposits are coarse textured and permeable, but variations in- the physical and hydrologic properties of a single deposit and from deposit to deposit are common. Ice-contact deposits are the source of the larger ground-water supplies in southeastern New Hampshire. \r\n\r\nMarine deposits underlie lowlands and valleys to a distance of about 20 miles inland from the present coastline. They commonly overlie bedrock and till and at places overlie or are interbedded with ice-contact deposits. Marine deposits range in thickness from less than 1 foot to possibly 75 feet. They are fine textured and impermeable; they do not yield water to wells in southeastern New Hampshire but generally act as a barrier to ground-water movement. Outwash and shore deposits form broad sand plains or gently sloping terraces of small extent. At most places the outwash and shore deposits, which range in thickness from less than 1 foot to about 50 feet, overlie marine deposits, but at some places they overlie bedrock, till, or ice-contact deposits. The outwash and shore deposits are fine textured and moderately permeable. They commonly yield enough ground water to meet the needs of farms, homes, and small industries. Alluvium underlies the flood plains and channels of the principal streams and overlies bedrock and older unconsolidated deposits wherever streams cross the older units. The alluvium generally is not tapped by wells. \r\n\r\nBeach deposits occupy areas along the Atlantic Ocean between promontories of bedrock or till. In general beach deposits are permeable and are a source of water supplies for domestic use. Yields of wells are limited, however, by the danger of drawing in salty water. \r\n\r\nRecharge in southeastern New Hampshire is derived principally from precipitation on outcrop areas of ice-contact deposits and outwash and shore deposits during the nongrowing season. Ground water is discharged naturally by springs, by effluent seepage to streams and other bodies of surface water, and by evapotranspiration. It ","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1695","usgsCitation":"Bradley, E., 1964, Geology and ground-water resources of southeastern New Hampshire: U.S. Geological Survey Water Supply Paper 1695, v, 80 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1695.","productDescription":"v, 80 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":25720,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25721,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25722,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25723,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25724,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25725,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25726,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1695/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25727,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1695/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137945,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1695/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685601","contributors":{"authors":[{"text":"Bradley, Edward","contributorId":67071,"corporation":false,"usgs":true,"family":"Bradley","given":"Edward","email":"","affiliations":[],"preferred":false,"id":143098,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1258,"text":"wsp1618 - 1964 - Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1618","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1618","title":"Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California","docAbstract":"The San Joaquin Valley includes roughly the southern two-thirds of the Central Valley of California, extending 250 miles from Stockton on the north to Grapevine at the foot of the Tehachapi Mountains. The valley floor ranges in width from 25 miles near Bakersfield to about 55 miles near Visalia; it has a surface area of about 10,000 square miles. More than one-quarter of all the ground water pumped for irrigation in the United States is used in this highly productive valley. Withdrawal of ground water from storage by heavy pumping not only provides a needed irrigation water supply, but it also lowers the ground-water level and makes storage space available in which to conserve excess water during periods of heavy runoff. A storage capacity estimated to be 93 million acre-feet to a depth of 200 feet is available in this ground-water reservoir. This is about nine times the combined capacity of the existing and proposed surface-water reservoirs in the San Joaquin Valley under the California Water Plan.\r\n\r\nThe landforms of the San Joaquin Valley include dissected uplands, low plains and fans, river flood plains and channels, and overflow lands and lake bottoms. Below the land surface, unconsolidated sediments derived from the surrounding mountain highlands extend downward for hundreds of feet. These unconsolidated deposits, consisting chiefly of alluvial deposits, but including some widespread lacustrine sediments, are the principal source of ground water in the valley. Ground water occurs under confined and unconfined conditions in the San Joaquin Valley. In much of the western, central, and southeastern parts of the valley, three distinct ground-water reservoirs are present. In downward succession these are 1) a body of unconfined and semiconfined fresh water in alluvial deposits of Recent, Pleistocene, and possibly later Pliocene age, overlying the Corcoran clay member of the Tulare formation; 2) a body of fresh water confined beneath the Corcoran clay member, which occurs in alluvial and lacustrine deposits of late Pliocene age or older; and 3) a body of saline connate water contained in marine sediments of middle Pliocene or older age, which underlies the fresh-water body throughout the area. In much of the eastern part of the valley, especially in the areas of the major streams, the Corcoran clay member is not present and ground water occurs as one fresh-water body to considerable depth.\r\n\r\nThe ground-water body is replenished by infiltration of rainfall, by infiltration from streams, canals, and ditches, by underflow entering the valley from tributary stream canyons, and by infiltration of excess irrigation water. In much of the valley, however, the annual rainfall is so low that little penetrates deeply, and soil-moisture deficiency is perennial. Infiltration from stream channels and canals and from irrigated fields are the principal sources of groundwater recharge. The ground-water storage capacity of the San Joaquin Valley has been estimated in an earlier report (Davis and others, 1959) as 93 million acre-feet. This is the quantity of water that would drain by gravity from the valley deposits if the regional water level were lowered from 10 to 200 feet below the land surface. Storage capacity was estimated for only the part of the valley considered to be potentially usable as a ground-water reservoir. In this study, a 200foot depth was selected as a practical valley-wide depth limit for unwatering \r\n\r\nunder full utilization of the ground-water reservoir, even though in localized areas sections in excess of 350 feet in depth have already been dewatered. Some of the factors that locally limit the utilization of the ground-water reservoir are inferior water quality, relatively impermeable surface soils, and relatively impermeable subsurface deposits. On the basis of a detailed analysis of la peg model, the subsurface geology of the San Joaquin Valley was subdivided into predominantly permeable and impermeable zones in the 1","language":"ENGLISH","publisher":"United States Govt. Print. Off.,","doi":"10.3133/wsp1618","usgsCitation":"Davis, G.H., Lofgren, B.E., and Mack, S., 1964, Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California: U.S. Geological Survey Water Supply Paper 1618, vii, 125 p. :illus., maps, diagrs., tables. and portfolio ;24 cm., https://doi.org/10.3133/wsp1618.","productDescription":"vii, 125 p. :illus., maps, diagrs., tables. and portfolio ;24 cm.","costCenters":[],"links":[{"id":137412,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1618/report-thumb.jpg"},{"id":26195,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26196,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26197,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26198,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26199,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26200,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26201,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26202,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26203,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26204,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26205,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26206,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1618/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604592","contributors":{"authors":[{"text":"Davis, G. H.","contributorId":40963,"corporation":false,"usgs":true,"family":"Davis","given":"G.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143449,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lofgren, B. E.","contributorId":42579,"corporation":false,"usgs":true,"family":"Lofgren","given":"B.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":143450,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mack, Seymour","contributorId":101247,"corporation":false,"usgs":true,"family":"Mack","given":"Seymour","email":"","affiliations":[],"preferred":false,"id":143451,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1122,"text":"wsp1773 - 1964 - Geology and ground-water resources of the Anchorage area, Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1773","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1773","title":"Geology and ground-water resources of the Anchorage area, Alaska","docAbstract":"The Anchorage area, at the head of Cook Inlet in south-central Alaska, \r\noccupies 150 square miles of a glaciated lowland and lies between two estuaries and the Chugach Mountains. Two military bases are in the area; \r\nAnchorage is the largest city in Alaska and the chief transportation center \r\nfor this part of the State. \r\nThe bedrock in the Anchorage area is chiefly Tertiary shale in the lowland \r\nand metamorphic rocks of Mesozoic age beneath the adjacent mountain \r\nslopes. Glacial drift which underlies nearly the entire area has an average \r\nthickness of several hundred feet and appears to include at least five sheets \r\nof deposits, two of which are exposed. The drift consists of till, outwash stream and lake deposits (sand and gravel), and estuarine (and lake) deposits \r\n(clay and silt). The stratigraphy and lateral distribution of the deposits are \r\ncomplex, but data at hand s, how that the thickest deposits, including all the \r\nestuarine and lake sediment and most of the stream-deposited sediment, \r\nare beneath the lowland away from the mountain wall, and that the deposits \r\nnear the mountains are till and subordinate outwash sediments. \r\nDeposits of sand and gravel laid down by outwash streams in channels and \r\non outwash plains are the most important aquifers, and the only \r\nones which yield large quantities of ground water from single beds. Thin \r\nlayers of sandy or gravelly material in till are also important aquifers although they yield relatively small quantities of water. Bedded sand and \r\nsilt associated with the estuarine and lake(?) clay commonly becomes unstable during drilling and pumping, and has been successfully developed in \r\nonly a few wells. Unconfined aquifers are extensive, but permeable saturated \r\nmaterial is thin in many places and water supplies available from them are \r\nsmall or undependable in those places. The most important aquifers are confined or artesian. Clay and till form the confining beds: the till is somewhat 'leaky' in many places. Near Anchorage the buried water-bearing \r\nbeds appear to be interconnected and to form a single artesian system. The \r\nwater table and piezometric surface slope from the mountain wall of the \r\nlowland toward the estuaries, and the flow of the ground water is in that \r\ndirection. The aquifers are recharged by the infiltration of precipitation \r\nat the land surface and of surface water through stream beds: near the mountains the artesian aquifers are probably recharged in part by percolation from \r\nthe water-table aquifer, and far from the mountains the water-table aquifer \r\nis probably recharged in part by upward flow from the underlying artesian \r\naquifers. In several valleys and in a few other places, in the lowland, artesian wells flow at the land surface. \r\nThe outwash sand and gravel are moderately to very permeable; most \r\nof the other water-bearing material are much less permeable. The co- efficient of transmissibility for some single beds of sandy gravel is as high \r\nas 60,000 to I00,000 gpd per ft (gallons per day per foot); for the entire \r\nsection of glacial drift at and near Anchorage it is believed to be of the \r\norder of 200,000 gpd per ft. Calculations based on this value for the total \r\nsection and on the slope of the piezometric surface indicate that in the \r\nimmediate vicinity of Anchorage about 5 million gpd flows through each \r\nmile-wide section of the drift (measured in a northeast-southwest direction, perpendicular to the direction of flow), under normal (nonpumping) conditions. Under conditions of continuous heavy pumping the slope of the piezometric surface is steepened, flow is increased, and additional recharge is induced. \r\n\r\nThe highest yield reported from a well in this area is 2.600 gpm (gallons per minute) with 35 feet of drawdown: the highest reported specific capacity is 180 gpm per ft of drawdown, for a well pumped at. 270 gpm. \r\n\r\nOnly a few wells in the area have been developed for high yields. Well screens have been used ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1773","usgsCitation":"Cederstrom, D.J., Trainer, F.W., and Waller, R.M., 1964, Geology and ground-water resources of the Anchorage area, Alaska: U.S. Geological Survey Water Supply Paper 1773, vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1773.","productDescription":"vi, 108 p. :illus., maps (1 col.) diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":138014,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1773/report-thumb.jpg"},{"id":25887,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25888,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25889,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25890,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1773/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25891,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1773/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6855f4","contributors":{"authors":[{"text":"Cederstrom, Dagfin John","contributorId":90287,"corporation":false,"usgs":true,"family":"Cederstrom","given":"Dagfin","email":"","middleInitial":"John","affiliations":[],"preferred":false,"id":143212,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trainer, Frank W.","contributorId":103655,"corporation":false,"usgs":true,"family":"Trainer","given":"Frank","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143213,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waller, Roger Milton","contributorId":22320,"corporation":false,"usgs":true,"family":"Waller","given":"Roger","email":"","middleInitial":"Milton","affiliations":[],"preferred":false,"id":143211,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","interactions":[{"subject":{"id":12513,"text":"ofr5027 - 1950 - Some exploration possibilities at the New Almaden quicksilver mine, Santa Clara County, California","indexId":"ofr5027","publicationYear":"1950","noYear":false,"title":"Some exploration possibilities at the New Almaden quicksilver mine, Santa Clara County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":1},{"subject":{"id":46936,"text":"ofr529 - 1952 - Eleven maps of the New Almanden quicksilver mine area, California","indexId":"ofr529","publicationYear":"1952","noYear":false,"title":"Eleven maps of the New Almanden quicksilver mine area, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":2},{"subject":{"id":50893,"text":"ofr4919 - 1949 - The New Almaden quicksilver mine, Santa Clara County, California","indexId":"ofr4919","publicationYear":"1949","noYear":false,"title":"The New Almaden quicksilver mine, Santa Clara County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":3},{"subject":{"id":55325,"text":"ofr4474 - 1941 - The Harry area, New Almaden mine, Santa Clara County, California","indexId":"ofr4474","publicationYear":"1941","noYear":false,"title":"The Harry area, New Almaden mine, Santa Clara County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5714,"text":"pp360 - 1964 - Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","indexId":"pp360","publicationYear":"1964","noYear":false,"title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California"},"id":4}],"lastModifiedDate":"2013-06-24T14:10:22","indexId":"pp360","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"360","title":"Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California","docAbstract":"The New Almaden district, situated a few miles south of San Jose in Santa Clara County, Calif., has yielded nearly 40 percent of the quicksilver produced in the United States. The area mapped as the district for this report includes about 80 square miles, extending south from the flat Santa Clara Valley across the moderately low foothills containing the mines to the more rugged crest of the California Coast Ranges.","language":"ENGLISH","publisher":"United States Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp360","usgsCitation":"Bailey, E.H., and Everhart, D.L., 1964, Geology and quicksilver deposits of the New Almaden district, Santa Clara County, California: U.S. Geological Survey Professional Paper 360, viii, 206 p., https://doi.org/10.3133/pp360.","productDescription":"viii, 206 p.","costCenters":[],"links":[{"id":104440,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4358.htm","linkFileType":{"id":5,"text":"html"},"description":"4358"},{"id":139893,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0360/report-thumb.jpg"},{"id":268949,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0360/report.pdf"}],"country":"United States","state":"California","county":"Santa Clara County","otherGeospatial":"New Almaden District","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -124,36 ], [ -124,39.5 ], [ -120,39.5 ], [ -120,36 ], [ -124,36 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6842a3","contributors":{"authors":[{"text":"Bailey, Edgar Herbert","contributorId":85179,"corporation":false,"usgs":true,"family":"Bailey","given":"Edgar","email":"","middleInitial":"Herbert","affiliations":[],"preferred":false,"id":151475,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Everhart, Donald Lough","contributorId":40108,"corporation":false,"usgs":true,"family":"Everhart","given":"Donald","email":"","middleInitial":"Lough","affiliations":[],"preferred":false,"id":151474,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3662,"text":"cir494 - 1964 - Ground water east of Jackson Lake, Grand Teton National Park, Wyoming","interactions":[],"lastModifiedDate":"2022-02-02T21:31:15.484531","indexId":"cir494","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","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":"494","title":"Ground water east of Jackson Lake, Grand Teton National Park, Wyoming","docAbstract":"The project area, which lies east of and adjacent to Jackson Lake is on the downthrown eastern block of the Teton fault, a normal fault that trends northward along the west edge of Jackson Lake. Rocks of pre-Cretaceous age are deeply buried beneath this area. Sedimentary rocks of Cretaceous age and sedimentary and volcanic rocks of Tertiary age, which have an aggregate thickness of about 30,000 feet, are exposed in the northern and eastern parts of the area. Along most of the east side of Jackson Lake, unconsolidated glacial and interglacial deposits of Quaternary age overlie the rocks of Cretaceous and Tertiary age. The unconsolidated deposits were penetrated by test drilling to a depth of 206 feet, but the maximum thickness is probably much greater. Test wells were drilled in five localities to evaluate the deposits of Quaternary age as possible sources of ground water for National Park Service facilities. In the Pilgrim Creek valley, test wells were capable of yielding 200 gpm (gallons per minute); properly constructed production wells could obtain much greater yields. Test wells at Lizard Point and Jackson Lake Campgrounds yielded more than 100 gpm, and a test well near the confluence of the Buffalo Fork and Snake rivers yielded 30 gpm. A test hole drilled in the NW1/4 sec. 36, T. 46 N., R. 115 W., was dry at 200 feet. Unconsolidated deposits of Quaternary age are the most promising source of additional ground water. Because of the extreme range in grain size and sorting, these deposits vary greatly in permeability. Their saturated thickness ranges from 0 to more than 130 feet and changes seasonally; variations of as much as 36 feet were measured (1961-62) in the Pilgrim Creek valley. In most localities where deposits of Quaternary age are ,present, small to moderate ground-water supplies can be developed; larger ground-water supplies can be developed in parts of the Pilgrim Creek valley. One well taps the Bivouac Formation of Late Pliocene or Pleistocene age, but no other wells are known to tap rocks of possible pre-Quaternary age. The Harebell Formation and Bacon Ridge Sandstone of Late Cretaceous age and the Bivouac Formation offer the best possibilities for development of additional water supplies from the consolidated rocks. Chemical analyses of water samples from 11 wells in the deposits of Quaternary age and 1 well in the Bivouac Formation indicate that the water is of generally good quality for drinking and most other purposes. Water from one well tapping lacustrine(?) sand had a dissolved-solids content of 321 ppm (parts per million); all other samples had from 87 to 145 ppm.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/cir494","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"McGreevy, L., and Gordon, E.D., 1964, Ground water east of Jackson Lake, Grand Teton National Park, Wyoming: U.S. Geological Survey Circular 494, Report: iv, 27 p.; 1 Plate: 16.90 x 21.58 inches, https://doi.org/10.3133/cir494.","productDescription":"Report: iv, 27 p.; 1 Plate: 16.90 x 21.58 inches","numberOfPages":"32","costCenters":[],"links":[{"id":395311,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_23905.htm"},{"id":30702,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/0494/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124436,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/0494/report-thumb.jpg"},{"id":271081,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/0494/plate-1.pdf"}],"country":"United States","state":"Wyoming","otherGeospatial":"Grand Teton National Park, Jackson Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.753173828125,\n 43.8008364060122\n ],\n [\n -110.753173828125,\n 44.067853669357596\n ],\n [\n -110.4345703125,\n 44.067853669357596\n ],\n [\n -110.4345703125,\n 43.8008364060122\n ],\n [\n -110.753173828125,\n 43.8008364060122\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66dc4f","contributors":{"authors":[{"text":"McGreevy, Laurence J.","contributorId":98706,"corporation":false,"usgs":true,"family":"McGreevy","given":"Laurence J.","affiliations":[],"preferred":false,"id":147362,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gordon, Ellis D.","contributorId":12451,"corporation":false,"usgs":true,"family":"Gordon","given":"Ellis","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":147361,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":52433,"text":"ofr64148 - 1964 - Effect of increased pumping of ground water in the Fairfield-New Baltimore area, Ohio--A prediction by analog model study","interactions":[],"lastModifiedDate":"2012-02-02T00:11:27","indexId":"ofr64148","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"64-148","title":"Effect of increased pumping of ground water in the Fairfield-New Baltimore area, Ohio--A prediction by analog model study","language":"ENGLISH","doi":"10.3133/ofr64148","usgsCitation":"Spieker, A.M., 1964, Effect of increased pumping of ground water in the Fairfield-New Baltimore area, Ohio--A prediction by analog model study: U.S. Geological Survey Open-File Report 64-148, 105 p., https://doi.org/10.3133/ofr64148.","productDescription":"105 p.","costCenters":[],"links":[{"id":179060,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db6255fb","contributors":{"authors":[{"text":"Spieker, A. M.","contributorId":22824,"corporation":false,"usgs":true,"family":"Spieker","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":245336,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":972,"text":"wsp1694 - 1964 - Geology and ground-water conditions in the Wilmington-Reading area, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1694","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1694","title":"Geology and ground-water conditions in the Wilmington-Reading area, Massachusetts","docAbstract":"The Wilmington-Reading area, as defined for this report, contains the headwaters of the Ipswich River in northeastern Massachusetts. Since World War II the growth of communities in this area and the change in character of some of them from rural to suburban have created new water problems and intensified old ones. The purpose of this report on ground-water conditions is to provide information that will aid in understanding and resolving some of these problems. \r\n\r\nThe regional climate, which is humid and temperate, assures the area an ample natural supply of water. At the current stage of water-resources development a large surplus of water drains from the area by way of the Ipswich River during late autumn, winter, and spring each year and is unavailable for use during summer and early autumn, when during some years there is a general water deficiency. \r\n\r\nGround water occurs both in bedrock and in the overlying deposits of glacial drift. The bedrock is a source of small but generally reliable supplies of water throughout the area. Glacial till also is a source of small supplies of water, but wells in till often fail to meet modern demands. Stratified glacial drift, including ice-contact deposits and outwash, yields small to large supplies of water. \r\n\r\nStratified glacial drift forms the principal ground-water reservoir. It partly fills a system of preglacial valleys corresponding roughly to the valleys of the present Ipswich River system and is more than 100 feet thick at places. The ice-contact deposits generally are more permeable than the outwash deposits. Ground water occurs basically under water-table conditions. \r\n\r\nRecharge in the Wilmington-Reading area is derived principally from precipitation on outcrop areas of ice-contact deposits and outwash during late autumn, winter. and spring. It is estimated that the net annual recharge averages about 10 inches and generally ranges from 5 inches during unusually dry years to 15 inches during unusually wet years. Ground water withdrawn largely by municipal wells supplies the towns of North Reading, Reading, and Wilmington. In 1957 the average daily withdrawal from these wells was about 2.5 million gallons, of which about half was used outside the Ipswich River drainage basin. \r\n\r\nThe chemical quality of the ground water is generally satisfactory except for local excessive concentrations of iron. \r\n\r\nThe storage capacity of the ground-water reservoir and recharge in the Wilmington-Reading area are large enough to sustain a total withdrawal of ground water at several times the current rate, but the use of the reservoir probably will be limited by the extent to which wells of moderate or large capacity can be dispersed. This will depend upon the distribution of areas of thick permeable materials. Conditions in the Martins Brook-Skug River drainage basin seem generally favorable for increased development of water supplies. In the rest of the Wilmington-Reading area the chances of finding substantial bodies of thick permeable materials probably are small, but further exploration is desirable. \r\n\r\nMeasures proposed to drain swampland by deepening and straightening the Ipswich River and its tributaries will have some effect upon the ground-water conditions. Probably the most obvious effect will be a lowering of water levels in wells near improved reaches of channel. Also important will b the effect of changes in low streamflow conditions on wells that induce infiltration from streams and the effect on well yields of an improved hydraulic connection between streams and the ground-water body. \r\n\r\nThe Reading 100-acre well field, which derives part of its supply by inducing recharge from the Ipswich River, would be affected by the drainage measures. During a dry summer, such as that of 1957, the flow of the Ipswich is fully diverted by pumping at this well field, and drawdowns at some of the wells approach half the saturated thickness of the aquifer there. If the drainage measures are","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1694","usgsCitation":"Baker, J.A., Healy, H., and Hackett, O.M., 1964, Geology and ground-water conditions in the Wilmington-Reading area, Massachusetts: U.S. Geological Survey Water Supply Paper 1694, v, 80 p. :ill., maps (1 col.) ;24 cm., https://doi.org/10.3133/wsp1694.","productDescription":"v, 80 p. :ill., maps (1 col.) ;24 cm.","costCenters":[],"links":[{"id":137045,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1694/report-thumb.jpg"},{"id":25518,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25519,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25520,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25521,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25522,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1694/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25523,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1694/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db6860c9","contributors":{"authors":[{"text":"Baker, John Augustus","contributorId":48159,"corporation":false,"usgs":true,"family":"Baker","given":"John","email":"","middleInitial":"Augustus","affiliations":[],"preferred":false,"id":142946,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Healy, H.G.","contributorId":72776,"corporation":false,"usgs":true,"family":"Healy","given":"H.G.","email":"","affiliations":[],"preferred":false,"id":142947,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hackett, O. M.","contributorId":38527,"corporation":false,"usgs":true,"family":"Hackett","given":"O.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":142945,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2021,"text":"wsp1668 - 1964 - Sediment transported by Georgia streams","interactions":[],"lastModifiedDate":"2017-02-01T09:16:21","indexId":"wsp1668","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1668","title":"Sediment transported by Georgia streams","docAbstract":"A reconnaissance investigation of the sediment transported by selected Georgia streams during the period December 1957 to June 1959 was made to provide a general understanding of the physical quality of stream water in Georgia and to supply facts needed in planning more detailed work. \r\n\r\nThe investigation was made by studying the variation of sediment concentration and sediment load with stream discharge at 33 sites and by relating the available data to topographic, geologic, climatic, and soil conditions in the State. In the Blue Ridge Mountains area of northern Georgia the great relief, moderately heavy precipitation, fast runoff, and loamy soils cause sediment concentrations and sediment loads which are above average for the State. During periods of moderate to low streamflow, the concentration of suspended sediment ranges from 1 to 25 ppm (parts per million). After heavy rainfall, sediment concentration increases rapidly as water discharge rises, and occasionally exceeds 1,000 ppm before decreasing again. The concentration may reach a maximum and decrease before the discharge peak is reached. A major part of the annual sediment load can be carried during a short period of time because of the great increase in both water discharge and sediment concentration during floods. The lower Coastal Plain differs from the mountainous areas in several respects. The topography is gently rolling to almost level, precipitation and runoff are less than average for the State, and topsoils generally consist of hard and loamy sand. Concentration of suspended sediment in streamflow commonly ranges from 1 to 20 ppm during periods of low to moderate discharge and increases to 15 to 60 ppm at high discharge. Because of the small increase in concentration with increasing stream discharge, the sediment load varies approximately in proportion to the discharge. \r\n\r\nThe sediment characteristics of streams in the Piedmont, the Valley and Ridge area. and the upper Coastal Plain are intermediate .between those of the Blue Ridge area and the lower Coastal Plain. \r\n\r\nComparison of suspended load with estimated bed load in a few Georgia streams suggests th.at bed load is less than 20 percent of the suspended load for most streams. \r\n\r\nFactors which appear to be most important in causing variation in sediment yield in Georgia are topographic relief, soil texture, and location of dams. Variations in other factors such as precipitation, runoff, covering vegetation, drainage area, and channel types serve to modify the effects of the major factors. \r\n\r\nIn general, Georgia stream water is of good quality. Water of some streams is of exceptionally fine quality and contains less than 30 ppm combined dissolved and suspended solids during at least 90 percent of the time. Knowledge of the nature and cause of variation in water quality will permit the most effective use of Georgia streams.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1668","usgsCitation":"Kennedy, V.C., 1964, Sediment transported by Georgia streams: U.S. Geological Survey Water Supply Paper 1668, vii, 101 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1668.","productDescription":"vii, 101 p. :ill., maps ;24 cm.","costCenters":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"links":[{"id":137613,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1668/report-thumb.jpg"},{"id":27488,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1668/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fbe4b07f02db5f4905","contributors":{"authors":[{"text":"Kennedy, Vance C.","contributorId":102063,"corporation":false,"usgs":true,"family":"Kennedy","given":"Vance","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":144541,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1219,"text":"wsp1693 - 1964 - A summary of the occurrence and development of ground water in the southern High Plains of Texas","interactions":[],"lastModifiedDate":"2022-12-30T22:35:11.105123","indexId":"wsp1693","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1693","title":"A summary of the occurrence and development of ground water in the southern High Plains of Texas","docAbstract":"The Southern High Plains of Texas occupies an area of about 22,000 square miles in northwest Texas, extending from the Canadian River southward. about 250 miles and from the New Mexico line eastward an average distance of about 120 miles.
The economy of the area is dependent largely upon irrigated agriculture, and in 1958 about 44,000 irrigation wells were in operation. The economy of the area is also dependent upon the oil industry either in the form of oil and gas production or in the form of industries based on the production of petroleum.
The Southern High Plains of Texas is characterized by a nearly flat land surface sloping gently toward the southeast at an average of 8 to 10 feet per mile. Shallow undrained depressions or playas are characteristic of the plains surface, and during periods of heavy rainfall, runoff collects in the depressions to form temporary ponds or lakes. Stream drainage on the plains surface is poorly developed; water discharges over the eastern escarpment off the plains only during periods of excessive rainfall.
The climate of the area is semiarid; the average annual precipitation is about 20 inches. About 70 percent of the precipitation falls during the growing season from April to September.
Rocks of Permian age underlie the entire area and consist chiefly of red sandstone and shale containing numerous beds of gypsum and dolomite. The Permian rocks are not a source of water in the Southern High Plains, and any water in these rocks would probably be saline.
The Triassic rocks underlying the Southern High Plains consist of three formations of the Dockum group: the Tecovas formation, the Santa Rosa sandstone. and the Chinle formation equivalent. The Tecovas and Chinle formation equivalent both consist chiefly of shale and sandy shale; however, the Santa Rosa sandstone consists mainly of medium to coarse conglomeratic sandstone containing some shale. The formations of the Dockum group are capable of yielding small to moderate quantities of water in many parts of the Southern High Plains; however, in practically all places the water is rather saline and probably unsuitable for most uses.
The Cretaceous formations in the Southern High Plains consist of several formations of the Trinity, Fredericksburg, and Washita groups. The rocks underlie a large part of the southern part of the Southern High Plains; they consist of sandstone, shale, and limestone, the sandstone and limestone being the principal water-bearing units. In a few places where the Cretaceous rocks appear to be in hydraulic connection with the overlying Ogallala formation, moderate quantities of water are obtained, particularly from the limestones. Locally the Cretaceous rocks may be important aquifers where other water is not available, but they generally do not constitute a large source of water for irrigation or municipal use.
The Ogallala formation of Pliocene age is the principal aquifer in the Southern High Plains of Texas; it supplies practically all the water used for all purposes. The formation is continuous throughout most of the Texas part of the Southern High Plains and extends into New Mexico. The .formation consists chiefly of sediments deposited by streams that had their headwaters in the mountainous regions to the west and northwest. The Ogallala formation rests unconformably upon an erosional surface of the underlying Triassic and Cretaceous rocks. The Ogallala consists of beds and lenses of clay, silt, sand, and gravel; caliche occurs as a secondary deposit ,in many places in the formation. In general the Ogallala is thicker in the northern part of the area; the thickness ranges from 400 to 500 feet in central Parmer, west-central Castro, and southwestern Floyd Counties to a knife edge where the formation wedges out against outcrops of the older rocks.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1693","usgsCitation":"Cronin, J., and Myers, B.N., 1964, A summary of the occurrence and development of ground water in the southern High Plains of Texas: U.S. Geological Survey Water Supply Paper 1693, Report: v, 88 p.; 7 Plates: 13.00 x 23.50 inches or smaller, https://doi.org/10.3133/wsp1693.","productDescription":"Report: v, 88 p.; 7 Plates: 13.00 x 23.50 inches or smaller","costCenters":[],"links":[{"id":26128,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26130,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26129,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26131,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":411263,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24899.htm","linkFileType":{"id":5,"text":"html"}},{"id":26127,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26132,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1693/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137997,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1693/report-thumb.jpg"},{"id":26126,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26125,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -99.9,\n 36.85\n ],\n [\n -104.481,\n 36.85\n ],\n [\n -104.481,\n 31.61\n ],\n [\n -99.9,\n 31.61\n ],\n [\n -99.9,\n 36.85\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a5f28","contributors":{"authors":[{"text":"Cronin, J.G.","contributorId":47769,"corporation":false,"usgs":true,"family":"Cronin","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":143387,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Myers, B. N.","contributorId":67490,"corporation":false,"usgs":true,"family":"Myers","given":"B.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":143388,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010470,"text":"70010470 - 1964 - Spalled, aerodynamically modified moldavite from Slavice, Moravia, Czechoslovakia","interactions":[],"lastModifiedDate":"2026-02-11T16:46:58.218961","indexId":"70010470","displayToPublicDate":"1964-11-06T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Spalled, aerodynamically modified moldavite from Slavice, Moravia, Czechoslovakia","docAbstract":"A Czechoslovakian tektite or moldavite shows clear, indirect evidence of aerodynamic ablation. This large tektite has the shape of a teardrop, with a strongly convex, deeply corroded, but clearly identifiable front and a planoconvex, relatively smooth, posterior surface. In spite of much erosion and corrosion, demarcation of the posterior and the anterior part of the specimen (the keel) is clearly preserved locally. This specimen provides the first tangible evidence that moldavites entered the atmosphere cold, probably at a velocity exceeding 5 kilometers per second; the result was selective heating of the anterior face and perhaps ablation during the second melting. This provides evidence of the extraterrestial origin of moldavites.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.146.3645.790","issn":"00368075","usgsCitation":"Chao, E.C., 1964, Spalled, aerodynamically modified moldavite from Slavice, Moravia, Czechoslovakia: Science, v. 146, no. 3645, p. 790-791, https://doi.org/10.1126/science.146.3645.790.","productDescription":"2 p.","startPage":"790","endPage":"791","costCenters":[],"links":[{"id":219075,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Czech Republic","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n 12.07683656894153,\n 51.37803979080644\n ],\n [\n 12.07683656894153,\n 48.516807647547694\n ],\n [\n 18.940933354965523,\n 48.516807647547694\n ],\n [\n 18.940933354965523,\n 51.37803979080644\n ],\n [\n 12.07683656894153,\n 51.37803979080644\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"146","issue":"3645","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b940ee4b08c986b31a834","contributors":{"authors":[{"text":"Chao, E. C. T.","contributorId":96713,"corporation":false,"usgs":true,"family":"Chao","given":"E.","email":"","middleInitial":"C. T.","affiliations":[],"preferred":false,"id":358993,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221902,"text":"70221902 - 1964 - Deep geothermal brine near Salton Sea, California","interactions":[],"lastModifiedDate":"2021-07-14T12:29:50.126423","indexId":"70221902","displayToPublicDate":"1964-07-14T07:27:05","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1093,"text":"Bulletin Volcanologique","active":true,"publicationSubtype":{"id":10}},"title":"Deep geothermal brine near Salton Sea, California","docAbstract":"A well drilled for geothermal power near Salton Sea in Imperial Valley, Calif., is 5,232 feet deep; it is the deepest well in the world (1962) in a high-temperature hot spring area. In the lower half of the hole temperatures are too high to measure with available equipment, but are at loast 270°C, and may be as much as 370°C. For comparison, maximum temperature heretofore reported at depth (1962) for hot spring areas is 295°C.
The well taps a very saline brine of Na-Ca-K-Cl type (about 185,000 ppm Cl) with exceptionally high potassium, and with the highest content of minor alkali elements known for natural waters; Fe, Mn, Zn, Pb, Cu, Ag, and some other metals are also exceptionally high. This brine may be connate, but present evidence favors a source in the magma chamber at depth that supplied late Quaternary rhyolite domes of the area. If the latter is correct, the brine is an undiluted magmatic water that is residual from the separation of a more volatile phase high in CO2, H2S, and with some alkali halides. Elsewhere, the hypothesized volatile phase may account for near-surface hot spring activity of most thermal areas of volcanic association. The residual brine of high salinity may ordinarily remain relatively deep in the volcanic systems because of high specific gravity and low content of volatiles, seldom appearing at the surface except in a greatly diluted form.
The hot springs of Arima, Japan, may be a rare example of this type of magmatic water discharging at the surface in moderate concentration (Cl as much as 42,000 ppm). Independent evidence from fluid inclusions in minerals of high-temperature base-metal deposits also favors the existence of magmatic water high in Na, Ca, and Cl, and low in CO2 and other volatile components.
During a three-month production test several tons of material precipitated in the horizontal discharge pipe from the well. Amorphous silica with iron and manganese, and bornite are the dominant recognized components. This material contains the astonishingly high contents of about 20 percent copper, 2 percent silver, and notable sulfur, arsenic, bismuth, lead, antimony, and some other minor elements. Total quantities of all elements in the original whole brine are not yet known, but calculated amounts corresponding to 1 to 3 ppm of copper and 0.1 to 0.3 ppm of silver were precipitated from the brine to form the pipe deposits. The brine, therefore, may be man’s first sample of an « active » ore solution.
Equally fascinating to many geologists is the possibility that in the lower part of the hole temperatures are so high and pressures are sufficient for young sedimentary rocks to be undergoing transformation into rocks with mineral assemblages of the greenschist facies of metamorphism. Drill cores from 4,400 to 5,000 feet in depth contain chlorite, albite, K-feldspar, epidote, mica, and quartz, with some indication of increase in metamorphic grade downward. Regional geological and geophysical studies favor a depth of about 20,000 feet to pre-Tertiary basement rocks in the general area. A shallow basement or local upfaulting of old metamorphic rocks are not likely possibilities for the thermal area.
","language":"English","publisher":"Springer","doi":"10.1007/BF02597534","usgsCitation":"White, D.E., 1964, Deep geothermal brine near Salton Sea, California: Bulletin Volcanologique, v. 27, p. 369-370, https://doi.org/10.1007/BF02597534.","productDescription":"2 p.","startPage":"369","endPage":"370","costCenters":[],"links":[{"id":387170,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Salton Sea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.16668701171875,\n 33.07082934859187\n ],\n [\n -115.55145263671876,\n 33.07082934859187\n ],\n [\n -115.55145263671876,\n 33.58259116393916\n ],\n [\n -116.16668701171875,\n 33.58259116393916\n ],\n [\n -116.16668701171875,\n 33.07082934859187\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"27","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"White, Donald E.","contributorId":76787,"corporation":false,"usgs":true,"family":"White","given":"Donald","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":819271,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221179,"text":"70221179 - 1964 - The father of modern ground water hydrology","interactions":[],"lastModifiedDate":"2021-06-04T17:17:06.636524","indexId":"70221179","displayToPublicDate":"1964-04-01T12:14:32","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"The father of modern ground water hydrology","docAbstract":"No abstract available.
","language":"English","publisher":"Elsevier","doi":"10.1111/j.1745-6584.1964.tb01749.x","usgsCitation":"Hackett, O.M., 1964, The father of modern ground water hydrology: Groundwater, v. 2, no. 2, p. 2-5, https://doi.org/10.1111/j.1745-6584.1964.tb01749.x.","productDescription":"4 p.","startPage":"2","endPage":"5","costCenters":[],"links":[{"id":386213,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"2","issue":"2","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Hackett, O. M.","contributorId":38527,"corporation":false,"usgs":true,"family":"Hackett","given":"O.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":816986,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221131,"text":"70221131 - 1964 - Radioelement dispersion in a sedimentary environment and its effect on uranium exploration","interactions":[],"lastModifiedDate":"2021-06-02T18:44:40.729852","indexId":"70221131","displayToPublicDate":"1964-03-01T13:40:47","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Radioelement dispersion in a sedimentary environment and its effect on uranium exploration","docAbstract":"The radioelement content of the major part of the southeast Texas Coastal Plain sedimentary sequence falls within a range common for sandstones and shales. Exceptions to the normal limit are mainly in small, widely scattered areas. One anomalous area, however, covers several tens of square miles and contains most of the important uranium deposits. Both mechanical and chemical dispersion of radioelements takes place in the immediate vicinity of the ore deposits, though no attempt is made to extend this local dispersion model to the large, regional gamma radiation anomaly. It is suggested that the point-source concept for sedimentary uranium deposits is unrealistic and that conventional aeroradiometric survey grid spacing can be substantially enlarged without seriously reducing efficiency in uranium exploration.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.59.2.309","usgsCitation":"Moxham, R., 1964, Radioelement dispersion in a sedimentary environment and its effect on uranium exploration: Economic Geology, v. 59, no. 2, p. 309-321, https://doi.org/10.2113/gsecongeo.59.2.309.","productDescription":"13 p.","startPage":"309","endPage":"321","costCenters":[],"links":[{"id":386146,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Texas","otherGeospatial":"southeast Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.84521484375,\n 29.76437737516313\n ],\n [\n -93.75732421875,\n 30.95876857077987\n ],\n [\n -96.48193359375,\n 30.35391637229704\n ],\n [\n -98.525390625,\n 29.036960648558267\n ],\n [\n -98.94287109375,\n 26.43122806450644\n ],\n [\n -97.119140625,\n 25.918526162075153\n ],\n [\n -93.84521484375,\n 29.76437737516313\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"59","issue":"2","noUsgsAuthors":false,"publicationDate":"1964-03-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Moxham, R.M.","contributorId":42234,"corporation":false,"usgs":true,"family":"Moxham","given":"R.M.","email":"","affiliations":[],"preferred":false,"id":816820,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221130,"text":"70221130 - 1964 - Radioelement dispersion in a sedimentary environment and its effect on uranium exploration","interactions":[],"lastModifiedDate":"2021-06-04T12:06:39.460624","indexId":"70221130","displayToPublicDate":"1964-03-01T13:40:47","publicationYear":"1964","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Radioelement dispersion in a sedimentary environment and its effect on uranium exploration","docAbstract":"The radioelement content of the major part of the southeast Texas Coastal Plain sedimentary sequence falls within a range common for sandstones and shales. Exceptions to the normal limit are mainly in small, widely scattered areas. One anomalous area, however, covers several tens of square miles and contains most of the important uranium deposits. Both mechanical and chemical dispersion of radioelements takes place in the immediate vicinity of the ore deposits, though no attempt is made to extend this local dispersion model to the large, regional gamma radiation anomaly. It is suggested that the point-source concept for sedimentary uranium deposits is unrealistic and that conventional aeroradiometric survey grid spacing can be substantially enlarged without seriously reducing efficiency in uranium exploration.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.59.2.309","usgsCitation":"Moxham, R., 1964, Radioelement dispersion in a sedimentary environment and its effect on uranium exploration: Economic Geology, v. 59, no. 2, p. 309-321, https://doi.org/10.2113/gsecongeo.59.2.309.","productDescription":"13 p.","startPage":"309","endPage":"321","costCenters":[],"links":[{"id":386192,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"59","issue":"2","noUsgsAuthors":false,"publicationDate":"1964-03-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Moxham, R.M.","contributorId":42234,"corporation":false,"usgs":true,"family":"Moxham","given":"R.M.","email":"","affiliations":[],"preferred":false,"id":816941,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}