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":2983,"text":"wsp1499E - 1964 - Water resources of the Flint area, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T15:45:12","indexId":"wsp1499E","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":"E","title":"Water resources of the Flint area, Michigan","docAbstract":"This report describes the water resources of Genesee County, Mich., whose principal city is Flint. The sources of water available to the county are the Flint and Shiawassee Rivers and their tributaries, inland lakes, ground water, and Lake Huron. The withdrawal use of water in the county in 1958 amounted to about 45 mgd. Of this amount, 36 mgd was withdrawn from the Flint River by the Flint public water-supply system. The rest was supplied by wells. At present (1959) the Shiawassee River and its tributaries and the inland lakes are not used for water supply.
Flint River water is used for domestic, industrial, and waste-dilution requirements in Flint. About 60 percent of the water supplied by the Flint public water system is used by Flint industry. At least 30 mgd of river water is needed for waste dilution in the Flint River during warm weather.
Water from Holloway Reservoir, which has a storage capacity of 5,760 million gallons, is used to supplement low flows in the Flint River to meet water-supply and waste-dilution requirements. About 650 million gallons in Kearsley Reservoir, on a Flint River tributary, is held in reserve for emergency use. Based on records for the lowest flows during the period 1930-52, the Flint River system, with the two reservoirs in operation, is capable of supplying about 60 mgd at Flint, less evaporation and seepage losses. The 1958 water demands exceeded this amount. Development of additional storage in the Flint River basin is unlikely because of lack of suitable storage sites. Plans are underway to supply Flint and most of Genesee County with water from Lake Huron.
The principal tributaries of the Flint River in and near Flint could furnish small supplies of water. Butternut Creek, with the largest flow of those studied, has an estimated firm yield of 0.054 mgd per sq mi for 95 percent of the time. The Shiawassee River at Byron is capable of supplying at least 29 mgd for 95 percent of the time.
Floods are a serious problem in Flint. The April 1947 flood, the largest on record, caused nearly $4 million flood damage in Flint. A proposed flood-control plan for Flint calls for channel, floodwall, and levee improvements and the removal or modification of some bridges.
Analyses of water samples taken from selected streams and lakes in the Flint area indicate that the waters are of the calcium bicarbonate type and generally hard to very hard. Flint River water is relatively uniform in quality although a progressive increase in iron, sodium, and chloride concentrations was noted between Otisville and Montrose. Downstream from Flint, the dissolved oxygen
content may be low during low flows. At times, concentrations of iron, manganese, phenols, color, and turbidity in Flint River water exceed the limits recommended in drinking water standards. Water temperatures ranged from freezing to 86°F in a 4-year period. The finished water supplied by the Flint water-treatment plant is fairly uniform in quality, moderately soft, alkaline, and low in color and turbidity. The pH is nearly always above 10. Further softening and removal of iron and related minerals would be desirable for certain industrial uses.
The quality of the water sampled in the Flint River tributaries was generally similar to that of the Flint River. However, no phenols or oils and waxes were found. Softening and other treatment dependent upon use would be required if these streams were developed for water supply.
Waters sampled in the Shiawassee River and selected lakes were generally less mineralized than Flint River water. Water from the lakes showed the lowest concentrations of dissolved solids. Softening would be required for nearly all uses. Additional treatment would depend upon contemplated use.
Shallow deposits of sand and gravel deposited as outwash along glacial meltwater streams and as deltas in the glacial lakes that covered the northwestern part of the county are sources of water to moderate- and large-capacity wells. Thick deposits of sand and gravel also fill some of the valleys in the bedrock surface and yield moderate to large supplies of water. Production from public supply wells tapping the drift aquifers in the area ranges from about 50 to 1,200 gpm. The water from the drift aquifer is hard or very hard and commonly contains objectionable amounts of iron.
The Saginaw formation is a source of water to wells supplying some of the small communities and industries in the county. The Saginaw, which is the uppermost bedrock formation in the area, underlies most of the county. It is composed of layers of sandstone, shale, and limestone and some beds of coal. The formation is composed principally of sandstone in some areas of the county, and shale in others. Production from wells tapping the Saginaw ranges from a few to about 500 gpm. The water produced is generally moderately hard or hard and commonly contains objectionable amounts of chloride. The quality of the water limits its development for water supply. Overdrafts from the Saginaw result in a lowering of the piezometric surface and commonly cause an upward migration of water high in chloride.
The Michigan and Marshall formations are generally not sources of fresh water where they are overlain by the Saginaw formation. In the southern and eastern parts of the county where they are overlain by glacial deposits, they are a source of water of good quality. The quantity of water obtainable from these formations is not fully known. However, the Marshall may be a source of large supplies of water in the southeastern part of the county.
An ample supply of water is available in lakes, ponds, and streams in the metropolitan area of Flint to meet requirements for domestic, sanitary, and firefighting use in civil defense emergencies. The extent of emergency use of water from these sources would depend upon the pumping, distribution, and treatment facilities available. Enough private industrial and commercial, and public wells are present in the area normally supplied by the Flint public water system to meet emergency requirements for domestic and sanitary use. Use of these wells would also depend upon available pumping and distribution facilities. Water from many of these wells contains objectionable amounts of chloride, but it could be used without treatment in an emergency.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1499E","usgsCitation":"Wiitala, S.W., Vanlier, K., and Krieger, R.A., 1964, Water resources of the Flint area, Michigan: U.S. Geological Survey Water Supply Paper 1499, Document: viii, 86 p.; 6 Plates: 20.00 x 18.29 inches or smaller, https://doi.org/10.3133/wsp1499E.","productDescription":"Document: viii, 86 p.; 6 Plates: 20.00 x 18.29 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":139431,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1499e/report-thumb.jpg"},{"id":29743,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29744,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29745,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29746,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29747,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29748,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1499e/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29749,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1499e/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","county":"Genesee County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-83.4607,43.2235],[-83.4593,43.1425],[-83.4589,43.1365],[-83.455,42.9681],[-83.4553,42.9617],[-83.4546,42.8798],[-83.4541,42.8766],[-83.5737,42.8744],[-83.6902,42.871],[-83.6863,42.7822],[-83.9225,42.7812],[-83.928,42.8677],[-83.9309,42.9574],[-83.9283,43.0451],[-83.9294,43.1334],[-83.9318,43.2204],[-83.8154,43.2212],[-83.694,43.2223],[-83.5809,43.2226],[-83.4607,43.2235]]]},\"properties\":{\"name\":\"Genesee\",\"state\":\"MI\"}}]}\n","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602df3","contributors":{"authors":[{"text":"Wiitala, Sulo Werner","contributorId":20315,"corporation":false,"usgs":true,"family":"Wiitala","given":"Sulo","email":"","middleInitial":"Werner","affiliations":[],"preferred":false,"id":146097,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vanlier, K.E.","contributorId":24332,"corporation":false,"usgs":true,"family":"Vanlier","given":"K.E.","affiliations":[],"preferred":false,"id":146098,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Krieger, Robert A.","contributorId":99954,"corporation":false,"usgs":true,"family":"Krieger","given":"Robert","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146099,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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 States","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"MultiPolygon\",\"coordinates\":[[[[-66.28243,18.51476],[-65.7713,18.42668],[-65.591,18.22803],[-65.84716,17.97591],[-66.59993,17.98182],[-67.18416,17.94655],[-67.24243,18.37446],[-67.10068,18.5206],[-66.28243,18.51476]]],[[[-155.54211,19.08348],[-155.68817,18.91619],[-155.93665,19.05939],[-155.90806,19.33888],[-156.07347,19.70294],[-156.02368,19.81422],[-155.85008,19.97729],[-155.91907,20.17395],[-155.86108,20.26721],[-155.78505,20.2487],[-155.40214,20.07975],[-155.22452,19.99302],[-155.06226,19.8591],[-154.80741,19.50871],[-154.83147,19.45328],[-155.22217,19.23972],[-155.54211,19.08348]]],[[[-156.07926,20.64397],[-156.41445,20.57241],[-156.58673,20.783],[-156.70167,20.8643],[-156.71055,20.92676],[-156.61258,21.01249],[-156.25711,20.91745],[-155.99566,20.76404],[-156.07926,20.64397]]],[[[-156.75824,21.17684],[-156.78933,21.06873],[-157.32521,21.09777],[-157.25027,21.21958],[-156.75824,21.17684]]],[[[-157.65283,21.32217],[-157.70703,21.26442],[-157.7786,21.27729],[-158.12667,21.31244],[-158.2538,21.53919],[-158.29265,21.57912],[-158.0252,21.71696],[-157.94161,21.65272],[-157.65283,21.32217]]],[[[-159.34512,21.982],[-159.46372,21.88299],[-159.80051,22.06533],[-159.74877,22.1382],[-159.5962,22.23618],[-159.36569,22.21494],[-159.34512,21.982]]],[[[-94.81758,49.38905],[-94.64,48.84],[-94.32914,48.67074],[-93.63087,48.60926],[-92.61,48.45],[-91.64,48.14],[-90.83,48.27],[-89.6,48.01],[-89.27292,48.01981],[-88.37811,48.30292],[-87.43979,47.94],[-86.46199,47.55334],[-85.65236,47.22022],[-84.87608,46.90008],[-84.77924,46.6371],[-84.54375,46.53868],[-84.6049,46.4396],[-84.3367,46.40877],[-84.14212,46.51223],[-84.09185,46.27542],[-83.89077,46.11693],[-83.61613,46.11693],[-83.46955,45.99469],[-83.59285,45.81689],[-82.55092,45.34752],[-82.33776,44.44],[-82.13764,43.57109],[-82.43,42.98],[-82.9,42.43],[-83.12,42.08],[-83.142,41.97568],[-83.02981,41.8328],[-82.69009,41.67511],[-82.43928,41.67511],[-81.27775,42.20903],[-80.24745,42.3662],[-78.93936,42.86361],[-78.92,42.965],[-79.01,43.27],[-79.17167,43.46634],[-78.72028,43.62509],[-77.73789,43.62906],[-76.82003,43.62878],[-76.5,44.01846],[-76.375,44.09631],[-75.31821,44.81645],[-74.867,45.00048],[-73.34783,45.00738],[-71.50506,45.0082],[-71.405,45.255],[-71.08482,45.30524],[-70.66,45.46],[-70.305,45.915],[-69.99997,46.69307],[-69.23722,47.44778],[-68.905,47.185],[-68.23444,47.35486],[-67.79046,47.06636],[-67.79134,45.70281],[-67.13741,45.13753],[-66.96466,44.8097],[-68.03252,44.3252],[-69.06,43.98],[-70.11617,43.68405],[-70.64548,43.09024],[-70.81489,42.8653],[-70.825,42.335],[-70.495,41.805],[-70.08,41.78],[-70.185,42.145],[-69.88497,41.92283],[-69.96503,41.63717],[-70.64,41.475],[-71.12039,41.49445],[-71.86,41.32],[-72.295,41.27],[-72.87643,41.22065],[-73.71,40.9311],[-72.24126,41.11948],[-71.945,40.93],[-73.345,40.63],[-73.982,40.628],[-73.95232,40.75075],[-74.25671,40.47351],[-73.96244,40.42763],[-74.17838,39.70926],[-74.90604,38.93954],[-74.98041,39.1964],[-75.20002,39.24845],[-75.52805,39.4985],[-75.32,38.96],[-75.07183,38.78203],[-75.05673,38.40412],[-75.37747,38.01551],[-75.94023,37.21689],[-76.03127,37.2566],[-75.72205,37.93705],[-76.23287,38.31921],[-76.35,39.15],[-76.54272,38.71762],[-76.32933,38.08326],[-76.99,38.23999],[-76.30162,37.91794],[-76.25874,36.9664],[-75.9718,36.89726],[-75.86804,36.55125],[-75.72749,35.55074],[-76.36318,34.80854],[-77.39763,34.51201],[-78.05496,33.92547],[-78.55435,33.86133],[-79.06067,33.49395],[-79.20357,33.15839],[-80.30132,32.50935],[-80.86498,32.0333],[-81.33629,31.44049],[-81.49042,30.72999],[-81.31371,30.03552],[-80.98,29.18],[-80.53558,28.47213],[-80.53,28.04],[-80.05654,26.88],[-80.08801,26.20576],[-80.13156,25.81677],[-80.38103,25.20616],[-80.68,25.08],[-81.17213,25.20126],[-81.33,25.64],[-81.71,25.87],[-82.24,26.73],[-82.70515,27.49504],[-82.85526,27.88624],[-82.65,28.55],[-82.93,29.1],[-83.70959,29.93656],[-84.1,30.09],[-85.10882,29.63615],[-85.28784,29.68612],[-85.7731,30.15261],[-86.4,30.4],[-87.53036,30.27433],[-88.41782,30.3849],[-89.18049,30.31598],[-89.59383,30.15999],[-89.41373,29.89419],[-89.43,29.48864],[-89.21767,29.29108],[-89.40823,29.15961],[-89.77928,29.30714],[-90.15463,29.11743],[-90.88022,29.14854],[-91.62678,29.677],[-92.49906,29.5523],[-93.22637,29.78375],[-93.84842,29.71363],[-94.69,29.48],[-95.60026,28.73863],[-96.59404,28.30748],[-97.14,27.83],[-97.37,27.38],[-97.38,26.69],[-97.33,26.21],[-97.14,25.87],[-97.53,25.84],[-98.24,26.06],[-99.02,26.37],[-99.3,26.84],[-99.52,27.54],[-100.11,28.11],[-100.45584,28.69612],[-100.9576,29.38071],[-101.6624,29.7793],[-102.48,29.76],[-103.11,28.97],[-103.94,29.27],[-104.45697,29.57196],[-104.70575,30.12173],[-105.03737,30.64402],[-105.63159,31.08383],[-106.1429,31.39995],[-106.50759,31.75452],[-108.24,31.75485],[-108.24194,31.34222],[-109.035,31.34194],[-111.02361,31.33472],[-113.30498,32.03914],[-114.815,32.52528],[-114.72139,32.72083],[-115.99135,32.61239],[-117.12776,32.53534],[-117.29594,33.04622],[-117.944,33.62124],[-118.4106,33.74091],[-118.51989,34.02778],[-119.081,34.078],[-119.43884,34.34848],[-120.36778,34.44711],[-120.62286,34.60855],[-120.74433,35.15686],[-121.71457,36.16153],[-122.54747,37.55176],[-122.51201,37.78339],[-122.95319,38.11371],[-123.7272,38.95166],[-123.86517,39.76699],[-124.39807,40.3132],[-124.17886,41.14202],[-124.2137,41.99964],[-124.53284,42.76599],[-124.14214,43.70838],[-124.02053,44.6159],[-123.89893,45.52341],[-124.07963,46.86475],[-124.39567,47.72017],[-124.68721,48.18443],[-124.5661,48.37971],[-123.12,48.04],[-122.58736,47.096],[-122.34,47.36],[-122.5,48.18],[-122.84,49],[-120,49],[-117.03121,49],[-116.04818,49],[-113,49],[-110.05,49],[-107.05,49],[-104.04826,48.99986],[-100.65,49],[-97.22872,49.0007],[-95.15907,49],[-95.15609,49.38425],[-94.81758,49.38905]]],[[[-153.00631,57.11584],[-154.00509,56.73468],[-154.5164,56.99275],[-154.67099,57.4612],[-153.76278,57.81657],[-153.22873,57.96897],[-152.56479,57.90143],[-152.14115,57.59106],[-153.00631,57.11584]]],[[[-165.57916,59.90999],[-166.19277,59.75444],[-166.84834,59.94141],[-167.45528,60.21307],[-166.46779,60.38417],[-165.67443,60.29361],[-165.57916,59.90999]]],[[[-171.73166,63.78252],[-171.11443,63.59219],[-170.49111,63.69498],[-169.68251,63.43112],[-168.68944,63.29751],[-168.77194,63.1886],[-169.52944,62.97693],[-170.29056,63.19444],[-170.67139,63.37582],[-171.55306,63.31779],[-171.79111,63.40585],[-171.73166,63.78252]]],[[[-155.06779,71.14778],[-154.34417,70.69641],[-153.90001,70.88999],[-152.21001,70.82999],[-152.27,70.60001],[-150.73999,70.43002],[-149.72,70.53001],[-147.61336,70.21403],[-145.68999,70.12001],[-144.92001,69.98999],[-143.58945,70.15251],[-142.07251,69.85194],[-140.98599,69.712],[-140.9925,66.00003],[-140.99777,60.3064],[-140.013,60.27684],[-139.039,60.00001],[-138.34089,59.56211],[-137.4525,58.905],[-136.47972,59.46389],[-135.47583,59.78778],[-134.945,59.27056],[-134.27111,58.86111],[-133.35555,58.41029],[-132.73042,57.69289],[-131.70781,56.55212],[-130.00778,55.91583],[-129.97999,55.285],[-130.53611,54.80275],[-131.08582,55.17891],[-131.96721,55.49778],[-132.25001,56.37],[-133.53918,57.17889],[-134.07806,58.12307],[-135.03821,58.18771],[-136.62806,58.21221],[-137.80001,58.5],[-139.86779,59.53776],[-140.82527,59.72752],[-142.57444,60.08445],[-143.95888,59.99918],[-145.92556,60.45861],[-147.11437,60.88466],[-148.22431,60.67299],[-148.01807,59.97833],[-148.57082,59.91417],[-149.72786,59.70566],[-150.60824,59.36821],[-151.71639,59.15582],[-151.85943,59.74498],[-151.40972,60.7258],[-150.34694,61.03359],[-150.62111,61.28442],[-151.89584,60.7272],[-152.57833,60.06166],[-154.01917,59.35028],[-153.28751,58.86473],[-154.23249,58.14637],[-155.30749,57.72779],[-156.30833,57.42277],[-156.5561,56.97998],[-158.11722,56.46361],[-158.43332,55.99415],[-159.60333,55.56669],[-160.28972,55.64358],[-161.22305,55.36473],[-162.23777,55.02419],[-163.06945,54.68974],[-164.78557,54.40417],[-164.94223,54.57222],[-163.84834,55.03943],[-162.87,55.34804],[-161.80417,55.89499],[-160.5636,56.00805],[-160.07056,56.41806],[-158.68444,57.01668],[-158.4611,57.21692],[-157.72277,57.57],[-157.55027,58.32833],[-157.04167,58.91888],[-158.19473,58.6158],[-158.51722,58.78778],[-159.05861,58.42419],[-159.71167,58.93139],[-159.98129,58.57255],[-160.35527,59.07112],[-161.355,58.67084],[-161.96889,58.67166],[-162.05499,59.26693],[-161.87417,59.63362],[-162.51806,59.98972],[-163.81834,59.79806],[-164.66222,60.26748],[-165.34639,60.5075],[-165.35083,61.0739],[-166.12138,61.50002],[-165.73445,62.075],[-164.91918,62.63308],[-164.56251,63.14638],[-163.75333,63.21945],[-163.06722,63.05946],[-162.26056,63.54194],[-161.53445,63.45582],[-160.77251,63.76611],[-160.95834,64.2228],[-161.51807,64.40279],[-160.77778,64.7886],[-161.39193,64.77724],[-162.45305,64.55944],[-162.75779,64.33861],[-163.54639,64.55916],[-164.96083,64.44695],[-166.42529,64.68667],[-166.845,65.0889],[-168.11056,65.67],[-166.70527,66.08832],[-164.47471,66.57666],[-163.65251,66.57666],[-163.7886,66.07721],[-161.67777,66.11612],[-162.48971,66.73557],[-163.71972,67.11639],[-164.43099,67.61634],[-165.39029,68.04277],[-166.76444,68.35888],[-166.20471,68.88303],[-164.43081,68.91554],[-163.16861,69.37111],[-162.93057,69.85806],[-161.9089,70.33333],[-160.9348,70.44769],[-159.03918,70.89164],[-158.11972,70.82472],[-156.58082,71.35776],[-155.06779,71.14778]]]]},\"properties\":{\"name\":\"United 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":1792,"text":"wsp1597 - 1964 - Geology and ground-water resources of the upper Grande Ronde River basin, Union County, Oregon","interactions":[],"lastModifiedDate":"2022-01-12T19:36:16.825771","indexId":"wsp1597","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":"1597","title":"Geology and ground-water resources of the upper Grande Ronde River basin, Union County, Oregon","docAbstract":"The upper Grande Ronde River basin is a 1,400-square-mile area in northeastern Oregon, between the Blue Mountains to the west and the Wallowa Mountains to the east. The area is drained by the Grande Ronde River, which flows northeast through this region and is tributary to the Snake River. The climate is generally moderate; temperature extremes recorded at La Grande are 22°F. below zero and 108°F. above. The average annual precipitation ranges from 13 to 20 inches in the Grande Ronde Valley to . more than 35 inches in the mountain highlands surrounding the valley. The topography of. the area is strongly controlled by the geologic structures, principally those related to block faulting. The terrain ranges from the nearly flat floors of the Grande Ronde and Indian Valleys, whose elevations are 2,600 to about 2,750 feet, to the mountainous uplands, whose average elevations are about 5,000 feet and which have local prominences exceeding 6,500 feet. The rocks in the upper Grande Ronde River basin, from oldest to youngest, are metamorphic rocks of pre-Tertiary age; igneous masses of diorite and granodiorite that intruded the metamorphic rocks; tuff-breccia, welded and silicified tuff, and andesite and dacite flows, of Tertiary age; the Columbia River basalt of Miocene and possibly early Pliocene age; fanglomerate and lacustrine deposits of Pliocene and Pleistocene age; and younger deposits . of alluvium, colluvium, and welded tuff. In the graben known as the Grande Ronde Valley, which is the principal populated district in the area, the valley fill deposits are as thick as 2,000 feet. The valley is bordered by the scarps of faults, the largest of which have displacements of more than 4.000 feet. Most of the wells in the area obtain small to moderate supplies of water from unconfined aquifers in the val1ey fill and alluvial fan deposits. Moderate to large quantities of water are obtained from aquifers carrying artesian water in the fan alluvium and the Columbia River basalt. The available supplies of ground water greatly exceed the relatively small amounts that are being used, and the natural supplies are ..adequate for foreseeable domestic, industrial, irrigation, and municipal. requirements. Yields of future wells probably could be improved appreciably over those of present wells by exercising close attention to subsurface conditions during construction, and by greater use of well screens, gravel envelopes, and well development techniques. The chemical quality of the ground water in general is excellent. All waters sampled are potable and are within the desired ranges of hardness and salinity for most public, industrial, and irrigation uses. The average temperature of shallow ground water drawn from, the alluvial fill was 3°F. above the mean annual air temperature. That of water obtained from the basalt is 6°F. above the temperatures computed from the 'normal' gradient of 1.8°F. per 100 feet of increased depth.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1597","usgsCitation":"Hampton, E.R., and Brown, S., 1964, Geology and ground-water resources of the upper Grande Ronde River basin, Union County, Oregon: U.S. Geological Survey Water Supply Paper 1597, Report: v, 99 p.; 6 Plates: 33.00 × 48.47 inches or smaller, https://doi.org/10.3133/wsp1597.","productDescription":"Report: v, 99 p.; 6 Plates: 33.00 × 48.47 inches or smaller","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":394258,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24786.htm"},{"id":26934,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1597/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26933,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1597/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26932,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1597/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26931,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1597/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26930,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1597/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137231,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1597/report-thumb.jpg"},{"id":26936,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1597/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26935,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1597/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Oregon","county":"Union County","otherGeospatial":"upper Grande Ronde River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.5,\n 45.083\n ],\n [\n -117.501,\n 45.083\n ],\n [\n -117.501,\n 45.592\n ],\n [\n -118.5,\n 45.592\n ],\n [\n -118.5,\n 45.083\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db6852c3","contributors":{"authors":[{"text":"Hampton, E. R.","contributorId":57038,"corporation":false,"usgs":true,"family":"Hampton","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144163,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brown, S. G.","contributorId":46914,"corporation":false,"usgs":true,"family":"Brown","given":"S. G.","affiliations":[],"preferred":false,"id":144162,"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":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":6428,"text":"pp483H - 1964 - Giant Upper Cretaceous oysters from the Gulf coast and Caribbean","interactions":[],"lastModifiedDate":"2014-08-05T13:28:30","indexId":"pp483H","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":"483","chapter":"H","title":"Giant Upper Cretaceous oysters from the Gulf coast and Caribbean","docAbstract":"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":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":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":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":2029,"text":"wsp1617A - 1964 - Discharge characteristics of embankment-shaped weirs","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1617A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1617","chapter":"A","title":"Discharge characteristics of embankment-shaped weirs","docAbstract":"An embankment-shaped weir is an embankment overtopped by flood waters. Among the engineering problems frequently resulting from. this occurrence is the need to compute the peak discharge from postflood yield observations. The research described in this. report was concerned with the theoretical and experimental bases for the computation procedure. \r\n\r\nThe research had two main objectives. One was to determine the relationship between embankment form and roughness and some of the more important discharge characteristics. The second was to define, theoretically and experimentally, the relationship between free-flow discharge and the boundary layer on the roadway. The first objective was accomplished with the experimental determination of coefficients of discharge and other significant flow characteristics for a variety of boundary and flow conditions. The second objective was accomplished with the development and experimental verification of a discharge equation which involved the boundary layer displacement thickness. This phase of the research included a general investigation of boundary layer growth on the roadway. \r\n\r\nIt is included that both free- and submerged-flow discharge are virtually independent of the influence of embankment shape and relative height. The influence of boundary resistance is appreciable only for smaller heads. The most practical solution for discharge is one which is based on. the simple weir equation and experimentally determined coefficients. A completely analytical equation of discharge is impractical. \r\n\r\nThe report contains the results of 936 experiments on the discharge characteristics of 17 different models; plus 106 boundary-layer velocity traverses on 4 different models. The data are summarized in both graphical and tabular form.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1617A","usgsCitation":"Kindsvater, C.E., 1964, Discharge characteristics of embankment-shaped weirs: U.S. Geological Survey Water Supply Paper 1617, v, 11 p. :tables, graphs, diagrs, illus. ;24 cm., https://doi.org/10.3133/wsp1617A.","productDescription":"v, 11 p. :tables, graphs, diagrs, illus. ;24 cm.","costCenters":[],"links":[{"id":137646,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1617a/report-thumb.jpg"},{"id":27502,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1617a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae939","contributors":{"authors":[{"text":"Kindsvater, Carl E.","contributorId":73182,"corporation":false,"usgs":true,"family":"Kindsvater","given":"Carl","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144552,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":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":2710,"text":"wsp1658 - 1964 - Ground-water resources of the South Platte River Basin in western Adams and southwestern Weld Counties, Colorado","interactions":[{"subject":{"id":56171,"text":"ofr5993 - 1959 - Investigation of the quality of ground water in the vicinity of Derby, Colorado","indexId":"ofr5993","publicationYear":"1959","noYear":false,"title":"Investigation of the quality of ground water in the vicinity of Derby, Colorado"},"predicate":"SUPERSEDED_BY","object":{"id":2710,"text":"wsp1658 - 1964 - Ground-water resources of the South Platte River Basin in western Adams and southwestern Weld Counties, Colorado","indexId":"wsp1658","publicationYear":"1964","noYear":false,"title":"Ground-water resources of the South Platte River Basin in western Adams and southwestern Weld Counties, Colorado"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:26","indexId":"wsp1658","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":"1658","title":"Ground-water resources of the South Platte River Basin in western Adams and southwestern Weld Counties, Colorado","docAbstract":"The area described in this report consists of about 970 square miles in western Adams and southwestern Weld Counties in northeastern Colorado. It includes that part of the South Platte River valley between Denver and Kuner, Colo., all of Beebe Draw, and the lower part of the valley of Box Elder Creek. The stream-valley lowlands are separated by rolling uplands. The climate is semiarid, the normal annual precipitation being about 13 inches; thus, irrigation is essential for stable agricultural development. The area contains about 220,000 acres of irrigated land in the stream valleys. Most of the remaining 400,000 acres of land is used for dry farming or grazing because it lacks irrigation water. Most of the lowlands were brought under irrigation with surface water during the early 1900's, and now nearly all the surface water in the area is appropriated for irrigation within and downstream from the area. Because the natural flow of the streams is sometimes less than the demand for water, ground water is used to supplement the surface-water supply. Wells, drilled chiefly since 1930, supply the supplemental water and in some places are the sole supply for irrigation use. \r\n\r\nRocks exposed in the area are of sedimentary origin and range in age from Lato Cretaceous to Recent. Those that are consolidated, called 'bedrock' in this report, consist of the Fox Hills sandstone and the Laramie and Arapahoe formations, all of Late Cretaceous age, and the Denver formation and Dawson arkose of Late Cretaceous and Tertiary age. The surface of the bedrock was shaped by ancestral streams, the valleys of which are reflected by the present surface topography. Dune sand, slope wash, and thin upland deposits of Quaternary age mantle the bedrock in the divide areas, and stream deposits ranging in thickness from 0 to about 125 feet partly fill the ancestral valleys. The valley-fill deposits consist of beds and lenses of clay, silt, sand, gravel, cobbles, and boulders. \r\n\r\nAbundant supplies of ground water for irrigation, municipal, and industrial use are obtained in the principal stream valleys from wells tapping valley-fill deposits beneath the flood plain and bordering terraces. Many domestic and stock wells obtain water from the unconsolidated deposits both on the uplands and in the valleys. The ground water in the valley-fill deposits generally is unconfined but in a few places is under slight artesian pressure. The bedrock formations yield small to moderate supplies of water to municipal, industrial, domestic, and stock wells, but the yields are not sufficient for irrigation. \r\n\r\nGround water in the South Platte River valley moves downstream and toward the river and is discharged into the river. The direction of ground-water movement in Beebe Draw and Box Elder Creek valley is nearly parallel to the streams. Beebe Seep, the stream in Beebe Draw, gains water from the groundwater reservoir in some reaches and loses water in others, but Box Elder Creek loses water to the ground-water reservoir throughout its course especially during floods. The shape and slope of the water table are affected chiefly by the permeability of the valley-fill deposits, the location and altitude of the areas of recharge and discharge, and the configuration of the underlying bedrock floor. The depth to water in the South Platte River valley ranges from less than 1 foot beneath the flood plain to as much as 80 feet beneath the terraces. In Beebe Draw the depth to water ranges from less than 1 foot to about 60 feet and in Box Elder Creek valley from about 5 feet to about 40 feet. During the period of record the annual fluctuation of water levels in wells in the area has ranged from 2 to 13 feet. Precipitation within the area and infiltrating water from irrigated tracts, reservoirs, canals, and streams are the principal sources of recharge to the ground-water reservoir; some recharge results from underflow from outside the area. Ground water is discharged by evapotranspiratio","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1658","usgsCitation":"Smith, R., Schneider, P., and Petri, L., 1964, Ground-water resources of the South Platte River Basin in western Adams and southwestern Weld Counties, Colorado: U.S. Geological Survey Water Supply Paper 1658, vi, 132 p. :ill., maps ;24 cm. +, https://doi.org/10.3133/wsp1658.","productDescription":"vi, 132 p. :ill., maps ;24 cm. +","costCenters":[],"links":[{"id":110003,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24850.htm","linkFileType":{"id":5,"text":"html"},"description":"24850"},{"id":138805,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1658/report-thumb.jpg"},{"id":29079,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29080,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29081,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29082,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29083,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29084,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29085,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29086,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29087,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29088,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1658/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29089,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1658/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db696a98","contributors":{"authors":[{"text":"Smith, Rex O.","contributorId":91088,"corporation":false,"usgs":true,"family":"Smith","given":"Rex O.","affiliations":[],"preferred":false,"id":145646,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schneider, P.A.","contributorId":56209,"corporation":false,"usgs":true,"family":"Schneider","given":"P.A.","email":"","affiliations":[],"preferred":false,"id":145645,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, Lester R.","contributorId":19534,"corporation":false,"usgs":true,"family":"Petri","given":"Lester R.","affiliations":[],"preferred":false,"id":145644,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2186,"text":"wsp1747 - 1964 - Geology and hydrology of the West Milton area, Saratoga County, New York","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1747","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1747","title":"Geology and hydrology of the West Milton area, Saratoga County, New York","docAbstract":"This report describes the geology, ground-water conditions, streamflow characteristics, and quality of water in the West Milton area, Saratoga County, N.Y. The West Milton area is in the east-central part of New York in the hilly region that forms a transition zone between the Adirondack Mountains and the Hudson-Mohawk valley lowland. Bedrock underlying the area consists of crystalline rocks of Precambrian age and sandstone, dolomite, limestone, and shale formations of Cambrian and Ordovician age. The formations have been moderately folded and have been displaced as much as several hundred feet' along at least three northeast-trending normal faults. The bedrock is overlain in nearly all parts of the area by a layer of unconsolidated deposits which ranges in thickness from a few feet to more than 200 feet. The unconsolidated deposits are of Pleistocene age and consist of unstratified materials (till) laid down by glacial ice at stratified sediments deposited by glacial meltwaters. The topography of the bedrock surface differs greatly from the topography of the land surface. Although not evident in the present topography, at least two channels, cut in bedrock by preglacial streams, pass through the area. \r\n\r\nGround-water supplies adequate to satisfy domestic requirements can be obtained from wells in any part of the area. Large ground-water supplies may be taken from coarse-grained stratified deposits comprising two aquifers in the valley of Kayaderosseras Creek. The Atomic Energy Commission has pumped as much as 1 mgd from a horizontal well drawing from the uppermost aquifer which is composed of flood-plain deposits. Part of the water yielded by this well during extended periods of pumping is induced flow from the creek. Three nearby vertical wells drilled by the Commission comprise a separate well field capable of yielding at least 2 mgd and possibly as much as 3 mgd from the deeper stratified deposits underlying the valley. A pumping test showed that at near the center of this well field the coefficient of transmissibility is about 125,000 gpd per ft and the coefficient of storage is about 0.0003. The water obtained from the sand and gravel has a hardness of about 125 ppm and contains about 150 ppm of dissolved solids. \r\n\r\nMost of the Government reservation is drained by Glowegee Creek, one of the larger tributaries of Kayaderosseras Creek. The average streamflow of Kayaderosseras Creek at West Milton is 141 cfs or about 1.5 cfs per sq. mi. The monthly mean discharge has ranged from a low of 21.7 cfs in September 1958 to a high of 866 cfs in March 1936, and the annual mean discharge has ranged from 94.5 cfs in 1941 to 198 cfs in 1952. The mean annual flood is 1,740 cfs and the 50-year flood is 5,300 cfs. \r\n\r\nStreamflow data have been collected on Glowegee Creek since 1948 at a station 0.5 mile south of West Milton. The average streamflow of Glowegee Creek at this station is 41 cfs or about 1.5 cfs per sq mi. The mean annual flood is 740 cfs and the 50-year flood is 2,250 cfs. \r\n\r\nThe quality of the water in both Kayaderosseras Creek and Glowegee Creek is satisfactory for public supply and most industrial purposes. The mineral content of both streams is low--the dissolved-solids content averaging about 93 ppm in Kayaderosseras Creek and about 131 ppm in Glowegee Creek. The average hardness of water in Kayaderosseras Creek and Glowegee Creek is 68 ppm and 102 ppm, respectively. During periods of low flow, suspended sediment discharge in both streams is less than 10 tons per day, but during periods of high flow, the sediment discharge has been as great as 163 tons per day in Glowegee Creek and 437 tons per day in Kayaderosseras Creek.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1747","usgsCitation":"Mack, F., Pauszek, F.H., and Crippen, J.R., 1964, Geology and hydrology of the West Milton area, Saratoga County, New York: U.S. Geological Survey Water Supply Paper 1747, viii, 110 p. :illus., maps, diagrs., tables. ;24 cm., https://doi.org/10.3133/wsp1747.","productDescription":"viii, 110 p. :illus., maps, diagrs., tables. ;24 cm.","costCenters":[],"links":[{"id":137741,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1747/report-thumb.jpg"},{"id":27816,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27817,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27818,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27819,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27820,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27821,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1747/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27815,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1747/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b4691","contributors":{"authors":[{"text":"Mack, Frederick K.","contributorId":95858,"corporation":false,"usgs":true,"family":"Mack","given":"Frederick K.","affiliations":[],"preferred":false,"id":144794,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pauszek, F. H.","contributorId":61399,"corporation":false,"usgs":true,"family":"Pauszek","given":"F.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":144793,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Crippen, John R.","contributorId":13208,"corporation":false,"usgs":true,"family":"Crippen","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144792,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1021,"text":"wsp1536I - 1964 - Methods of determining permeability, transmissibility and drawdown","interactions":[{"subject":{"id":51650,"text":"ofr5480 - 1954 - The \"slug test\" for estimating transmissibility","indexId":"ofr5480","publicationYear":"1954","noYear":false,"title":"The \"slug test\" for estimating transmissibility"},"predicate":"SUPERSEDED_BY","object":{"id":1021,"text":"wsp1536I - 1964 - Methods of determining permeability, transmissibility and drawdown","indexId":"wsp1536I","publicationYear":"1964","noYear":false,"chapter":"I","title":"Methods of determining permeability, transmissibility and drawdown"},"id":1},{"subject":{"id":51779,"text":"ofr54310 - 1954 - Estimating transmissibility from specific capacity","indexId":"ofr54310","publicationYear":"1954","noYear":false,"title":"Estimating transmissibility from specific capacity"},"predicate":"SUPERSEDED_BY","object":{"id":1021,"text":"wsp1536I - 1964 - Methods of determining permeability, transmissibility and drawdown","indexId":"wsp1536I","publicationYear":"1964","noYear":false,"chapter":"I","title":"Methods of determining permeability, transmissibility and drawdown"},"id":2}],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1536I","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":"1536","chapter":"I","title":"Methods of determining permeability, transmissibility and drawdown","docAbstract":"If the Theis graphical method is used for determining the hydraulic constants of an aquifer under water-table conditions, the observed drawdowns should be corrected for the decrease in saturated thickness. This is especially true if the drawdown is a large fraction of the original saturated thickness, for then the computed coefficient of permeability is highly inaccurate if based on observed, rather than corrected, water levels. Wenzel's limiting formula, a modification of the Theis graphical method, is useful where u=r2s/4Tt is less than about 0.01. However, a shorter procedure for determination of the coefficient of transmissibility, as well as the coefficient of storage, consists of plotting the values of the corrected drawdowns against the values of the logarithm of r. \r\n\r\nWenzel (1942) suggested that observation wells be situated on lines that extend upgradient and downgradient from the pumped well. However, a detailed analysis of aquifer-test results indicates that such a restriction is unnecessary. The gradient method for determining permeability should yield the same results as the Thies method. The former, when applied for a distance within the range of applicability of the latter, is merely a duplication of effort or, at best, a crude check. Because of the limitations of accuracy in plotting, the gradient method is much less satisfactory. That Wenzel (1942) obtained identical results from the two methods is regarded as a coincidence. \r\n\r\nFailure to take into consideration the fact that the pumped well does not tap the full thickness of the aquifer leads to an apparent coefficient of permeability that is much too low, especially if the aquifer consists of stratified sediments. The average coefficient of permeability computed from uncorrected drawdowns may be only a little more than half of the true value.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1536I","usgsCitation":"Bentall, R., 1964, Methods of determining permeability, transmissibility and drawdown: U.S. Geological Survey Water Supply Paper 1536, vi, 99 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1536I.","productDescription":"vi, 99 p. :ill. ;24 cm.","costCenters":[],"links":[{"id":137921,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1536i/report-thumb.jpg"},{"id":25635,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1536i/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a54e4b07f02db62bcc6","contributors":{"authors":[{"text":"Bentall, Ray","contributorId":78711,"corporation":false,"usgs":true,"family":"Bentall","given":"Ray","email":"","affiliations":[],"preferred":false,"id":143040,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"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 States","state":"Georgia","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-84.810477,34.987607],[-83.619985,34.986592],[-83.620185,34.992091],[-83.108714,35.000768],[-83.1046,34.992783],[-83.106991,34.98272],[-83.120387,34.968406],[-83.12114,34.958966],[-83.127035,34.953778],[-83.120502,34.941262],[-83.122585,34.938062],[-83.12807,34.938113],[-83.140621,34.924915],[-83.153253,34.926342],[-83.160937,34.918269],[-83.168524,34.91788],[-83.186541,34.899534],[-83.203351,34.893717],[-83.201183,34.884653],[-83.205627,34.880142],[-83.213323,34.882796],[-83.220099,34.878124],[-83.23751,34.877057],[-83.238419,34.869771],[-83.245602,34.865522],[-83.255718,34.845592],[-83.267656,34.845289],[-83.268159,34.821393],[-83.275656,34.816862],[-83.289914,34.824477],[-83.294292,34.814725],[-83.301368,34.814154],[-83.301182,34.804008],[-83.313782,34.799911],[-83.323866,34.789712],[-83.320062,34.759616],[-83.348829,34.737194],[-83.353238,34.728648],[-83.349411,34.697575],[-83.339029,34.683807],[-83.321463,34.677543],[-83.316401,34.669316],[-83.304641,34.669561],[-83.292883,34.654196],[-83.27796,34.644853],[-83.255281,34.637696],[-83.240669,34.624507],[-83.243381,34.617997],[-83.23178,34.611297],[-83.169994,34.605444],[-83.170278,34.592398],[-83.154577,34.588198],[-83.152577,34.578299],[-83.122901,34.560129],[-83.103987,34.540166],[-83.103176,34.533406],[-83.084855,34.530967],[-83.078113,34.524837],[-83.086861,34.517798],[-83.069451,34.502131],[-83.054463,34.50289],[-83.034712,34.483495],[-83.002924,34.472132],[-82.99509,34.472483],[-82.992671,34.479072],[-82.979568,34.482702],[-82.960668,34.482002],[-82.954667,34.477302],[-82.940867,34.486102],[-82.922866,34.481402],[-82.902665,34.485902],[-82.876864,34.475303],[-82.873831,34.471508],[-82.876464,34.465803],[-82.862156,34.458748],[-82.855762,34.443977],[-82.835004,34.366069],[-82.795223,34.34096],[-82.780308,34.296701],[-82.746656,34.266407],[-82.74192,34.210063],[-82.732761,34.195338],[-82.730824,34.175906],[-82.717507,34.150504],[-82.70414,34.141007],[-82.67732,34.131657],[-82.659077,34.103544],[-82.641553,34.092212],[-82.64398,34.072237],[-82.635991,34.064941],[-82.626963,34.063457],[-82.609655,34.039917],[-82.596155,34.030517],[-82.589245,34.000118],[-82.57554,33.992049],[-82.579576,33.979761],[-82.569864,33.970684],[-82.556835,33.945353],[-82.543128,33.940949],[-82.526741,33.943765],[-82.51295,33.936969],[-82.492929,33.909754],[-82.455105,33.88165],[-82.422803,33.863754],[-82.403881,33.865477],[-82.371775,33.843813],[-82.32448,33.820033],[-82.300213,33.800627],[-82.298286,33.783518],[-82.285804,33.780058],[-82.247472,33.752591],[-82.239098,33.730872],[-82.234576,33.700216],[-82.200718,33.66464],[-82.196583,33.630582],[-82.186154,33.62088],[-82.174351,33.613117],[-82.158331,33.60971],[-82.142872,33.594278],[-82.12908,33.589925],[-82.116545,33.596485],[-82.10624,33.595637],[-82.096352,33.58407],[-82.046335,33.56383],[-82.033023,33.546454],[-82.001338,33.520135],[-81.985938,33.486536],[-81.926336,33.462937],[-81.913356,33.437418],[-81.926789,33.426576],[-81.919217,33.413126],[-81.9373,33.401259],[-81.925737,33.37114],[-81.930634,33.368165],[-81.939637,33.37254],[-81.946337,33.37064],[-81.944737,33.364041],[-81.934837,33.356041],[-81.939737,33.344941],[-81.917973,33.34159],[-81.919137,33.334442],[-81.909285,33.324181],[-81.898187,33.329664],[-81.884137,33.310443],[-81.875836,33.307443],[-81.870436,33.312943],[-81.847296,33.306783],[-81.849636,33.299544],[-81.861536,33.297944],[-81.863236,33.288844],[-81.838257,33.272975],[-81.838337,33.269098],[-81.847336,33.266345],[-81.852136,33.247544],[-81.827936,33.228746],[-81.811736,33.223847],[-81.805236,33.211447],[-81.784535,33.208147],[-81.778935,33.209847],[-81.778435,33.221847],[-81.768935,33.217447],[-81.758235,33.200248],[-81.760635,33.189248],[-81.772435,33.181249],[-81.763135,33.159449],[-81.743835,33.14145],[-81.704634,33.116451],[-81.683533,33.112651],[-81.646433,33.094552],[-81.614298,33.094661],[-81.609476,33.089862],[-81.610078,33.082883],[-81.600211,33.083966],[-81.600091,33.073497],[-81.583804,33.067021],[-81.57288,33.05418],[-81.562066,33.055568],[-81.558336,33.046183],[-81.54251,33.045254],[-81.540081,33.040613],[-81.513231,33.028546],[-81.492253,33.009342],[-81.494736,32.978998],[-81.499471,32.96478],[-81.506449,32.962423],[-81.508436,32.955765],[-81.499446,32.944988],[-81.502427,32.935353],[-81.483198,32.921802],[-81.479184,32.905638],[-81.464069,32.897814],[-81.479445,32.881082],[-81.45392,32.874074],[-81.453949,32.849761],[-81.444866,32.850967],[-81.426475,32.840773],[-81.417984,32.818196],[-81.423772,32.810514],[-81.428313,32.78311],[-81.421128,32.778039],[-81.426481,32.770291],[-81.417606,32.762684],[-81.410845,32.741694],[-81.418542,32.732586],[-81.421194,32.711978],[-81.427517,32.701896],[-81.4131,32.692648],[-81.41075,32.694772],[-81.401256,32.680156],[-81.405273,32.656517],[-81.393818,32.653491],[-81.403582,32.643398],[-81.407271,32.631737],[-81.413411,32.637368],[-81.41866,32.629392],[-81.389338,32.595436],[-81.380999,32.589652],[-81.369757,32.591231],[-81.366964,32.577059],[-81.328753,32.561228],[-81.29676,32.562648],[-81.281324,32.556464],[-81.275213,32.545202],[-81.277131,32.535417],[-81.252882,32.51833],[-81.237095,32.517314],[-81.234023,32.513778],[-81.238281,32.505988],[-81.233585,32.498488],[-81.200029,32.467985],[-81.186829,32.464086],[-81.203046,32.448844],[-81.201595,32.44136],[-81.207246,32.437542],[-81.20513,32.423788],[-81.177231,32.39169],[-81.181072,32.380398],[-81.169332,32.369436],[-81.170858,32.362722],[-81.155136,32.34717],[-81.144032,32.351093],[-81.133632,32.341293],[-81.135733,32.324594],[-81.122933,32.307295],[-81.121433,32.284496],[-81.145834,32.263397],[-81.155995,32.241478],[-81.136727,32.213669],[-81.128283,32.208634],[-81.118234,32.189201],[-81.119361,32.177142],[-81.129634,32.165602],[-81.123134,32.162902],[-81.120034,32.153303],[-81.117234,32.117605],[-81.113334,32.113205],[-81.093386,32.11123],[-81.066906,32.090351],[-81.050234,32.085308],[-81.032674,32.08545],[-81.011961,32.100176],[-81.002297,32.100048],[-80.983133,32.079609],[-80.954482,32.068622],[-80.922794,32.039151],[-80.885517,32.0346],[-80.859111,32.023693],[-80.852276,32.026676],[-80.84313,32.024226],[-80.840549,32.011306],[-80.848441,31.988279],[-80.862814,31.969346],[-80.897687,31.949065],[-80.911207,31.943769],[-80.929101,31.944964],[-80.930279,31.956705],[-80.948491,31.95723],[-80.972392,31.94127],[-80.975714,31.923602],[-80.968494,31.915822],[-80.934508,31.90918],[-80.99269,31.857641],[-81.000317,31.856744],[-81.014478,31.867474],[-81.041548,31.876198],[-81.065255,31.877095],[-81.05907,31.850106],[-81.076178,31.836132],[-81.075812,31.829031],[-81.057181,31.822687],[-81.039808,31.823],[-81.036873,31.812721],[-81.077057,31.761256],[-81.097402,31.753126],[-81.130634,31.722692],[-81.138448,31.720934],[-81.192784,31.733245],[-81.203572,31.719448],[-81.186303,31.701509],[-81.161084,31.691401],[-81.151888,31.698411],[-81.139394,31.699917],[-81.131137,31.695774],[-81.136408,31.674832],[-81.131728,31.654484],[-81.133493,31.623348],[-81.160364,31.570436],[-81.173079,31.555908],[-81.178822,31.55553],[-81.186114,31.568032],[-81.204315,31.568183],[-81.214536,31.557601],[-81.240699,31.552313],[-81.254218,31.55594],[-81.260076,31.54828],[-81.263905,31.532579],[-81.258809,31.52906],[-81.217948,31.527284],[-81.199518,31.537596],[-81.181592,31.527697],[-81.177254,31.517074],[-81.189643,31.503588],[-81.204883,31.473124],[-81.246911,31.422784],[-81.278798,31.367214],[-81.282923,31.326491],[-81.268027,31.324218],[-81.25482,31.315452],[-81.274688,31.289454],[-81.276862,31.254734],[-81.289136,31.225487],[-81.288403,31.211065],[-81.293359,31.206332],[-81.314183,31.207938],[-81.339028,31.186918],[-81.35488,31.167204],[-81.360791,31.155903],[-81.359349,31.149166],[-81.368241,31.136534],[-81.399677,31.134113],[-81.403732,31.107115],[-81.401267,31.072781],[-81.420474,31.016703],[-81.432475,31.012991],[-81.434923,31.017804],[-81.451444,31.015515],[-81.469298,30.996028],[-81.490586,30.984952],[-81.493651,30.977528],[-81.486966,30.969602],[-81.475789,30.965976],[-81.466814,30.97091],[-81.453568,30.965573],[-81.447388,30.956732],[-81.426929,30.956615],[-81.420108,30.974076],[-81.408484,30.977718],[-81.403409,30.957914],[-81.405153,30.908203],[-81.428577,30.836336],[-81.446927,30.81039],[-81.460061,30.769912],[-81.45947,30.741979],[-81.444124,30.709714],[-81.472597,30.713312],[-81.487332,30.726081],[-81.528278,30.723359],[-81.540923,30.713343],[-81.561706,30.715597],[-81.571419,30.721636],[-81.601206,30.728141],[-81.607667,30.721924],[-81.617663,30.722046],[-81.625098,30.733017],[-81.646137,30.727591],[-81.65177,30.732284],[-81.651723,30.740235],[-81.662173,30.746521],[-81.672824,30.738935],[-81.688925,30.741434],[-81.692815,30.7471],[-81.719927,30.744634],[-81.732227,30.749634],[-81.747572,30.766455],[-81.763372,30.77382],[-81.779171,30.768062],[-81.792769,30.784432],[-81.806652,30.789683],[-81.840375,30.786384],[-81.852626,30.794439],[-81.868608,30.792754],[-81.89572,30.821098],[-81.910926,30.815889],[-81.949787,30.827493],[-81.962175,30.818001],[-81.962534,30.796526],[-81.973856,30.778487],[-81.988605,30.780056],[-82.007865,30.792937],[-82.022866,30.787991],[-82.024035,30.783156],[-82.011597,30.763122],[-82.017917,30.755263],[-82.038967,30.749262],[-82.043795,30.729641],[-82.036426,30.706585],[-82.050432,30.676266],[-82.049507,30.655548],[-82.042271,30.649452],[-82.039941,30.637144],[-82.028499,30.621829],[-82.027338,30.606726],[-82.016503,30.602484],[-82.012109,30.593773],[-82.005477,30.563495],[-82.018361,30.531184],[-82.01477,30.513009],[-82.017779,30.475081],[-82.037209,30.434518],[-82.034005,30.422357],[-82.04199,30.403266],[-82.036825,30.377884],[-82.047917,30.363265],[-82.060034,30.360328],[-82.094687,30.360781],[-82.104834,30.368319],[-82.161757,30.357851],[-82.170054,30.358929],[-82.19294,30.378779],[-82.210291,30.42459],[-82.203975,30.444507],[-82.207708,30.460503],[-82.200938,30.474438],[-82.201416,30.485164],[-82.226933,30.510281],[-82.23582,30.537187],[-82.231916,30.55627],[-82.214385,30.566958],[-83.499876,30.645671],[-84.86346,30.711506],[-84.896122,30.750591],[-84.914322,30.753591],[-84.920123,30.76599],[-84.917423,30.77589],[-84.928323,30.79309],[-84.927923,30.80279],[-84.936042,30.820671],[-84.928335,30.844263],[-84.935256,30.854328],[-84.935413,30.882481],[-84.966726,30.917287],[-84.971026,30.928187],[-84.983127,30.934786],[-84.979627,30.954686],[-84.982527,30.965586],[-85.005931,30.97704],[-84.999428,31.013843],[-85.009409,31.032378],[-85.011392,31.053546],[-85.028573,31.074583],[-85.026068,31.08418],[-85.029736,31.096163],[-85.035615,31.108192],[-85.054677,31.120818],[-85.064028,31.142495],[-85.076628,31.156927],[-85.100207,31.16549],[-85.098426,31.17777],[-85.106503,31.185305],[-85.106963,31.202693],[-85.09977,31.209751],[-85.096763,31.225651],[-85.111711,31.258022],[-85.114548,31.276302],[-85.110309,31.281733],[-85.099107,31.284165],[-85.089774,31.295026],[-85.084152,31.328313],[-85.088983,31.334292],[-85.085918,31.353146],[-85.09099,31.354428],[-85.092487,31.362881],[-85.078641,31.39636],[-85.079978,31.410472],[-85.074762,31.424879],[-85.06697,31.428594],[-85.071621,31.468384],[-85.045642,31.516813],[-85.047196,31.528671],[-85.041305,31.540987],[-85.05796,31.57084],[-85.055976,31.605178],[-85.060418,31.611271],[-85.057473,31.618624],[-85.082829,31.637967],[-85.083545,31.656071],[-85.092429,31.659966],[-85.12553,31.694965],[-85.12653,31.716764],[-85.11913,31.730964],[-85.129231,31.758663],[-85.12523,31.767063],[-85.140431,31.779663],[-85.132231,31.795162],[-85.131331,31.817562],[-85.141831,31.839261],[-85.138331,31.844161],[-85.140131,31.858761],[-85.128831,31.87636],[-85.132931,31.89306],[-85.114031,31.89336],[-85.10803,31.90516],[-85.112731,31.909859],[-85.07893,31.940159],[-85.08683,31.957758],[-85.067829,31.967358],[-85.07093,31.981658],[-85.068098,31.991857],[-85.064544,32.002489],[-85.053815,32.013502],[-85.05883,32.046656],[-85.055491,32.072657],[-85.047063,32.090433],[-85.06206,32.132486],[-85.045593,32.143758],[-85.011267,32.180493],[-84.966828,32.193952],[-84.966346,32.208034],[-84.957057,32.21671],[-84.925427,32.221551],[-84.912488,32.247463],[-84.890894,32.261504],[-84.9338,32.29826],[-85.001874,32.322015],[-85.007103,32.328362],[-85.004582,32.345196],[-84.983466,32.363186],[-84.976767,32.392648],[-84.981098,32.402833],[-84.979431,32.412244],[-84.96343,32.422544],[-84.967031,32.435343],[-84.971831,32.442843],[-84.995331,32.453243],[-84.998231,32.469842],[-84.994831,32.486042],[-85.0071,32.523868],[-85.015805,32.528428],[-85.022509,32.542923],[-85.067535,32.579546],[-85.076399,32.594665],[-85.08224,32.616264],[-85.088319,32.623032],[-85.087294,32.634407],[-85.098259,32.642708],[-85.089736,32.655635],[-85.093536,32.669734],[-85.114737,32.685634],[-85.122738,32.715727],[-85.1202,32.737647],[-85.138101,32.753836],[-85.133275,32.780609],[-85.167939,32.811612],[-85.168342,32.828516],[-85.159309,32.841382],[-85.160792,32.848466],[-85.177127,32.853895],[-85.1844,32.861317],[-85.42947,34.125096],[-85.561416,34.750079],[-85.605165,34.984678],[-84.810477,34.987607]]]},\"properties\":{\"name\":\"Georgia\",\"nation\":\"USA \"}}]}","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":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":12938,"text":"ofr6433 - 1964 - Geology of the Andover Granite and surrounding rocks, Massachusetts","interactions":[],"lastModifiedDate":"2012-02-02T00:06:56","indexId":"ofr6433","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":"64-33","title":"Geology of the Andover Granite and surrounding rocks, Massachusetts","docAbstract":"Field and petrographic studies of the Andover Granite and surrounding rocks have afforded an opportunity for an explanation of its emplacement and crystallization. The investigation has contributed secondarily to an understanding of the geologic history of southeastern New England, particularly as it is revealed in the Lawrence, Wilmington, South Groveland, and Reading quadrangles of Massachusetts. \r\n\r\nThe Andover Granite and Sharpners Pond Tonalite together comprise up to 90 percent of the Acadian(?) subalkaline intrusive series cropping out within the area of study. The subalkaline series locally invades a sequence of early to middle Paleozoic and possibly Precambrian metasedimentary and metavolcanic rocks. Much of the subalkaline series and most of the Andover Granite is confined between two prominent east-northeast trending faults or fault systems. The northern fault separates the mildly metamorphosed Middle Silurian(?) Merrimack Group on the north from a highly metamorphosed and thoroughly intruded Ordovician(?) sequence on the south. The southern 'boundary '' fault is a major structural discontinuity characterized by penetrative, diffuse shearing over a zone one-half mile or more in width. \r\n\r\nThe magmatic nature of the Andover Granite is demonstrated by: (1) sharply crosscutting relationships with surrounding rocks; (2) the occurrence of tabular-shaped xenoliths whose long directions parallel the foliation within the granite and whose internal foliation trends at a high angle to that of the granite; (3) continuity with the clearly intrusive Sharpners Pond Tonalite; (4) the compositional uniformity of the granite as contrasted with the compositional diversity of the rocks it invades; (5) its modal and normative correspondence with (a) calculated norms of salic extrusives and (b) that of the ternary (\u001Cgranite\u001D) minimum for the system NaAlSi3O8-KAlSi3O8-SiO2. \r\n\r\nOrogenic granites, as represented by the Andover, contrast with post-orogenic granites, represented locally by the Peabody Granite, in their phase composition and texture. Unlike the Peabody, the Andover Granite is thought to have been thoroughly recrystallized through the unmixing of initially homogeneous phases with the concomitant development of extremely intricate, allotriomorphic textures. Textural relationships between potassium and plagioclase feldspars and among quartz and the two feldspars, suggest that the Andover Granite has evolved through exsolution of a single hypersolvus feldspar (or two coexisting subsolvus feldspars of only slightly disparate compositions) into discrete grains of plagioclase and potassium feldspar, much along the lines proposed by Tuttle (1952). \r\n\r\nA hypothesis is proposed for the origin of myrmekite whereby it is evolved indirectly through exsolution of a homogeneous, hypersolvus, calcalkali feldspar in the presence of a silica reservoir. Where the An 'molecule' is contained in the primary mix crystal, exsolution into potassium and plagioclase feldspar phases normally requires a paired exchange between Ca-Al and K-Si. Should the silicon requirements of the developing potassium feldspar be met by the matrix silica reservoir, the concomitantly evolving plagioclase may become stoichiometrically enriched in silicon and ultimately develop into myrmekite. Discrete unmixing of pure alkali feldspar proceeds through simple alkali ion exchange; ternary compostions high in An are more apt to fall initially in the two-feldspar field, thereby reducing the unmixing potential. General restriction of myrmekite to plagioclase of calcic albite to oligoclase composition is explained accordingly.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6433","usgsCitation":"Castle, R.O., 1964, Geology of the Andover Granite and surrounding rocks, Massachusetts: U.S. Geological Survey Open-File Report 64-33, 550 p. ill., maps ;29 cm., https://doi.org/10.3133/ofr6433.","productDescription":"550 p. ill., maps ;29 cm.","costCenters":[],"links":[{"id":146979,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0033/report-thumb.jpg"},{"id":41382,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41383,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41384,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41385,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41386,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41387,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41388,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41389,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41390,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0033/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41391,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0033/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db68353e","contributors":{"authors":[{"text":"Castle, Robert O.","contributorId":22741,"corporation":false,"usgs":true,"family":"Castle","given":"Robert","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":166992,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16256,"text":"ofr64151 - 1964 - Magnetic properties of Pd, Pd-H and Pd-D from 300 degrees K to 4.2 degrees K","interactions":[],"lastModifiedDate":"2024-08-05T20:04:29.494955","indexId":"ofr64151","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":"64-151","title":"Magnetic properties of Pd, Pd-H and Pd-D from 300 degrees K to 4.2 degrees K","docAbstract":"The magnetic properties of many substances first studied seriously by Faraday have played an important role in our modern technology. In particular, the magnetic properties of the transition elements are of great importance in the understanding of the electronic band form of these elements. Once the electronic band form is known, many of the physical properties may be predicted. Although many investigations have been made of the magnetic properties of palladium, no recent measurements have been reported at temperatures lower than 20° K.
There is some discrepancy between the earlier work of Onnes and Oosterhuis (1913, 1914) and the later work of Hoare and Matthews (1952). There is reason to believe that the later work is correct because of the purity of the samples, but the data indicate a necessity for measurements at temperatures below 20° K.
Palladium adsorbs enormous amounts of hydrogen and a study of this effect could lead to information which would be valuable in the interpretation of the magnetic properties of palladium. The magnetic susceptibility of hydrogenized palladium was studied first by Graham (1869). Since that time it has been shown by Svensson (1953) that the susceptibility of palladium diminishes linearly with increasing hydrogen content and finally reaches a value just below zero for a H/pd volume ratio of 800/1. This same effect was shown to occur by Sieverts and Danz (1937) when deuterium is substituted for hydrogen. Recently, Wucher (1952) has made a study of the variation of the susceptibility of hydrogenized palladium with temperature from -98.6° C to 16.3° C. However, later measurements of the resistivity and thermoelectric power of hydrogenized palladium by Schindler and Smith (1979) indicate that there might be a magnetic anomaly in hydrogenized palladium at 40° K.
The purpose of this work is to extend the previous measurements down to 4.2° K, but measurements will be made on desorbed as well as adsorbed samples of hydrogenized and deuterized palladium. The results on the desorbed samples turned out to be quite interesting and suggest further experiments.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr64151","usgsCitation":"Thorpe, A.N., 1964, Magnetic properties of Pd, Pd-H and Pd-D from 300 degrees K to 4.2 degrees K: U.S. Geological Survey Open-File Report 64-151, 56 p., https://doi.org/10.3133/ofr64151.","productDescription":"56 p.","costCenters":[],"links":[{"id":148285,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0151/report-thumb.jpg"},{"id":432173,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0151/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649328","contributors":{"authors":[{"text":"Thorpe, Arthur N.","contributorId":52591,"corporation":false,"usgs":true,"family":"Thorpe","given":"Arthur","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":172505,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12674,"text":"ofr6413 - 1964 - Reconnaissance geochemistry of stream sediments from three areas near Juneau, Alaska","interactions":[],"lastModifiedDate":"2023-12-20T20:19:32.865407","indexId":"ofr6413","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":"64-13","title":"Reconnaissance geochemistry of stream sediments from three areas near Juneau, Alaska","docAbstract":"Results of a preliminary inquiry into background metal content of stream sediments near Juneau, Alaska, and whether this background is related to geologic terrane indicate that stream sediments derived chiefly from metamorphic rocks show significantly higher modal nickel, zinc, and arsenic than do sediments derived mainly from sedimentary or igneous rocks. Metal-content data that are closely related to areal geology will be required before systematic geochemical prospecting by stream-sediment sampling in southeast Alaska will be very effective.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6413","usgsCitation":"Berg, H., 1964, Reconnaissance geochemistry of stream sediments from three areas near Juneau, Alaska: U.S. Geological Survey Open-File Report 64-13, 6 p., https://doi.org/10.3133/ofr6413.","productDescription":"6 p.","costCenters":[],"links":[{"id":423814,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0013/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":145691,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0013/report-thumb.jpg"}],"country":"United States","state":"Alaska","city":"Juneau","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -134.772259154342,\n 58.50149487777199\n ],\n [\n -134.772259154342,\n 58.17857516496329\n ],\n [\n -134.00321618559198,\n 58.17857516496329\n ],\n [\n -134.00321618559198,\n 58.50149487777199\n ],\n [\n -134.772259154342,\n 58.50149487777199\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a73e4b07f02db643ba1","contributors":{"authors":[{"text":"Berg, Henry C.","contributorId":73176,"corporation":false,"usgs":true,"family":"Berg","given":"Henry C.","affiliations":[],"preferred":false,"id":166526,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"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":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":2659,"text":"wsp1608F - 1964 - Cenomanian-Turonian aquifer of central Israel, its development and possible use as a storage reservoir","interactions":[],"lastModifiedDate":"2013-08-12T12:29:21","indexId":"wsp1608F","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":"1608","chapter":"F","title":"Cenomanian-Turonian aquifer of central Israel, its development and possible use as a storage reservoir","docAbstract":"The Cenomanian-Turonian formations constitute a highly permeable dolomite and limestone aquifer in central Israel. The aquifer is on the west limb of an anticlinorium that trends north-northeast. In places it may be as much as 800 meters thick, but in the report area, largely the foothills of the Judean-Ephraim Mountains where the water development is most intensive, its thickness is generally considerably less. In some places the aquifer occurs at or near the land surface, or it is covered by sandy and gravelly coastal-plain deposits. However, in a large part of the area, it is overlain by as much as 400 meters of relatively impermeable strata, and it is probably underlain by less permeable Lower Cretaceous strata. \n\nIn general the aquifer water is under artesian pressure. The porosity of the aquifer is characterized mainly by solution channels and cavities produced by jointing and faulting. In addition to the generally high permeability of the aquifer, some regions, which probably coincide with ancient drainage patterns and (or) fault zones, have exceptionally high permeabilities. \n\nThe source of most of the water in the aquifer is believed to be rain that falls on the foothills area. The westward movement of ground water from the mountainous outcrop areas appears to be impeded by a zone of low permeability which is related to structural and stratigraphic conditions along the western side of the mountains. \n\nGradients of the piezometric surface are small, and the net direction of water movement is westward and northwestward under natural conditions. Locally, however, the flow pattern may be in other directions owing to spatial variations in permeability in the aquifer, the location of natural discharge outlets, and the relation of the aquifer to adjacent geologic formations. There probably is also a large vertical component of flow. \n\nPumping has modified the flow pattern by producing several irregularly shaped shallow depressions in the piezometric surface although, to date, no unwatering of the aquifer has occurred. In the central part of the area, pumping has induced some infiltration from overlying coastal-plain formations. \n\nInjecting and storing surplus water seasonally in the aquifer should be feasible at almost any place. However, the movement and recovery of the injected water probably could be controlled most easily if the water were injected where depressions have been formed in the piezometric surface.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608F","usgsCitation":"Schneider, R., 1964, Cenomanian-Turonian aquifer of central Israel, its development and possible use as a storage reservoir: U.S. Geological Survey Water Supply Paper 1608, iii, 20 p. :ill. ;24 cm. + plates folded in pocket., https://doi.org/10.3133/wsp1608F.","productDescription":"iii, 20 p. :ill. ;24 cm. + plates folded in pocket.","costCenters":[],"links":[{"id":138224,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608f/report-thumb.jpg"},{"id":28995,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":276493,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608f/plate-2.pdf"},{"id":276494,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608f/plate-3.pdf"},{"id":276492,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608f/plate-1.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6f54","contributors":{"authors":[{"text":"Schneider, Robert","contributorId":102460,"corporation":false,"usgs":true,"family":"Schneider","given":"Robert","email":"","affiliations":[],"preferred":false,"id":145569,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1154,"text":"wsp1779S - 1964 - Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada","interactions":[],"lastModifiedDate":"2012-02-02T00:05:12","indexId":"wsp1779S","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":"1779","chapter":"S","title":"Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada","docAbstract":"Practically all the ground water of economic importance in the Truckee Meadows area, an alluviated intermontane basin in western Nevada is in the valley fill, which consists of unconsolidated and partially consolidated sedimentary deposits. The Mesozoic and Cenozoic consolidated rocks of the mountains bordering the valley contain some water in fractures and other openings, but they have virtually no interstitial permeability. The permeability of the valley fill is extremely variable. The Truckee Formation, which is the oldest deposit of the valley fill, yields very little water to wells. Permeable lenses of sand and gravel in the valley fill that are younger than the Truckee Formation yield moderate to large amounts of water to wells. \r\n\r\nThe estimated average annual recharge to and discharge from the groundwater reservoir is 35,000 acre-feet. About 25,000 acre-feet of the recharge is from the infiltration of irrigation water diverted from the Truckee River. Most of the discharge is by evapotranspiration and by seepage to ditches and streams. \r\n\r\nSome water in the area is unsuitable for many uses because of its poor chemical quality. Water in the Steamboat Springs area is hot and has high concentrations of chloride and dissolved solids. Both water draining areas of bleached rock and ground water downgradient from areas of leached rock have high concentrations of sulfate and dissolved solids. Surface water of low dissolved-solids content mixes with and dilutes some highly mineralized ground water. \r\n\r\nIncreased pumping in discharge areas will help to alleviate waterlogged conditions and will decrease ground-water losses by evapotranspiration. Increased pumping near the Truckee River may induce recharge from the river to the ground-water system.","language":"ENGLISH","publisher":"U.S. Government Printing Office,","doi":"10.3133/wsp1779S","usgsCitation":"Cohen, P.M., and Loeltz, O.J., 1964, Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada: U.S. Geological Survey Water Supply Paper 1779, v, 63 p. :ill., maps ;23 cm., https://doi.org/10.3133/wsp1779S.","productDescription":"v, 63 p. :ill., maps ;23 cm.","costCenters":[],"links":[{"id":137311,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1779s/report-thumb.jpg"},{"id":25954,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25955,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25956,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1779s/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25957,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1779s/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ae4b07f02db6250cd","contributors":{"authors":[{"text":"Cohen, Philip M.","contributorId":67860,"corporation":false,"usgs":true,"family":"Cohen","given":"Philip","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143269,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Loeltz, Omar J.","contributorId":86312,"corporation":false,"usgs":true,"family":"Loeltz","given":"Omar","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":143270,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}