Rock County is in south-central Wisconsin adjacent to the Illinois State line. The county has an area of about 723 square miles and had a population of about 113,000 in 1957 ; it is one of the leading agricultural and industrial counties in the State. The total annual precipitation averages about 32 inches, and the mean annual temperature is about 48 ? F. Land-surface altitudes are generally between 800 and 00 feet, but range from 731 feet, where the Rock River flows into Illinois, to above 1,080 feet, at several places in the northwestern part of the county. The northern part of Rock County consists of the hills and kettles of a terminal moraine which slopes southward to a flat, undissected outwash plain. The southeastern part of the county is an area of gentle slopes, whereas the southwestern part consists of steep-sided valleys and ridges. Rock County is within the drainage basin of the Rock River, which flows southward through the center of the county. The western and southwestern parts of ,the county are drained by the Sugar River und Coon Creek, both of which flow into the Pecatonica River in Illinois and thence into the Rock River. The southeastern part of the county is drained by Turtle Creek, which also flows into Illinois before joining the Rock River. Nearly all the lakes and ponds are in the northern one-third of the county, the area of most recent glaciation. The aquifers in Rock County are of sedimentary origin and include deeply buried sandstones, shales, and dolomites of the Upper Cambrian series. This series overlies crystalline rocks of Precambrian age and supplies water to all the cities and villages in the county. The St. Peter sandstone of Ordovician age underlies all Rock County except where the formation has been removed by erosion in the Rock and Sugar River valleys, and perhaps in Coon Creek valley. The St. Peter sandstone is the principal source of water for domestic, stock, and small industrial wells in the western half of the county. This sandstone also yields some water to uncased wells that tap the deeper rocks of the Upper Cambrian series. East of the Rock River the Platteville, Decorah, and Galena formations undifferentiated, or Platteville-Galena unit, is the principal source of water for domestic and stock wells. Unconsolidated deposits of glacial origin cover most of Rock County and supply water to many small wells. In the outwash deposits along the Rock River, wells of extremely high capacity have been developed for industrial and municipal use. The most significant feature of the bedrock surface in Rock County is the ancestral Rock River valley, which has been filled with glacial outwash to a depth of at least 396 feet below the present land surface. East of the buried valley the bedrock has a fiat, relatively undissected surface. West of the valley the bedrock surface is rugged and greatly dissected. Ground water in Rock County occurs under both water-table and artesian conditions; however, because of the interconnection and close relation of all ground water in the county, the entire system is considered to be a single groundwater body whose surface may be represented by one piezometric map. Recharge occurs locally, throughout the county. Nearly all recharge is derived directly from precipitation that percolates downward to become a part of the groundwater body. Natural movement of water in the consolidated water-bearing units is generally toward the buried Rock and Sugar River valleys. Movement of water in the sandstones of Cambrian age was calculated to be about 44 million gallons a day toward the Rock River. Discharge from wells in Rock County in 1957 was about 23 million gallons a day. Nearly 90 percent of this water was drawn from the area along the Rock River. Drilled wells, most of which were drilled by the cable-tool method, range in diameter from 3 to 26 inches, and in depth from 46 to 1,225 feet. Driven wells in alluvium and glacial drift are usually 1? to 2? in
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1619X","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey","usgsCitation":"LeRoux, E.F., 1964, Geology and ground-water resources of Rock County, Wisconsin: U.S. Geological Survey Water Supply Paper 1619, Report: iv, 50 p.; 5 Plates: 36.5 x 28.75 inches or smaller, https://doi.org/10.3133/wsp1619X.","productDescription":"Report: iv, 50 p.; 5 Plates: 36.5 x 28.75 inches or smaller","numberOfPages":"50","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":27697,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619x/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27698,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619x/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27699,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619x/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27700,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619x/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27701,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1619x/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27702,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1619x/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138328,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1619x/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Rock County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-89.0119,42.8471],[-88.8951,42.8457],[-88.7757,42.8455],[-88.7753,42.7587],[-88.7744,42.6728],[-88.774,42.5855],[-88.7737,42.4958],[-88.9385,42.4984],[-88.9798,42.4989],[-89.0467,42.4997],[-89.154,42.501],[-89.2345,42.5018],[-89.2705,42.5021],[-89.3185,42.5024],[-89.3645,42.5029],[-89.3656,42.5907],[-89.3656,42.5998],[-89.3667,42.677],[-89.3666,42.6906],[-89.3671,42.7607],[-89.3677,42.7743],[-89.3689,42.8484],[-89.2488,42.8478],[-89.132,42.8479],[-89.0119,42.8471]]]},\"properties\":{\"name\":\"Rock\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db6859c5","contributors":{"authors":[{"text":"LeRoux, E. F.","contributorId":29795,"corporation":false,"usgs":true,"family":"LeRoux","given":"E.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":144694,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":35469,"text":"b1161D - 1964 - Geologic reconnaissance of the Antelope-Ashwood area, north-central Oregon, with emphasis on the John Day Formation of late Oligocene and early Miocene age","interactions":[],"lastModifiedDate":"2022-07-05T21:10:38.994709","indexId":"b1161D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1161","chapter":"D","title":"Geologic reconnaissance of the Antelope-Ashwood area, north-central Oregon, with emphasis on the John Day Formation of late Oligocene and early Miocene age","docAbstract":"This report briefly describes the geology of an area of about 750 square miles in Jefferson, Wasco, Crook, and Wheeler Counties, Oregon. About 16,000 feet of strata that range in age from pre-Tertiary to Quaternary are exposed. These include the following units: pre-Tertiary slate, graywacke, conglomerate, and meta-andesite; Clarno Formation of Eocene age - lava flows, volcanic breccia, tuff, and tuffaceous mudstone, chiefly of andesitic composition; John Day Formation of late Oligocene and early Miocene age - pyroclastic rocks, flows, and domes, chiefly of rhyolitic composition; Columbia River Basalt of middle Miocene age - thick, columnar jointed flows of very fine grained dense dark-gray basalt; Dalles Formation of Pliocene age - bedded tuffaceous sandstone, siltstone, and conglomerate; basalt of Pliocene or Pleistocene age - lava flows of porous-textured olivine basalt; and Quaternary loess, landslide debris, and alluvium. Unconformities separate pre-Tertiary rocks and Clarno Formation, Clarno and John Day Formations, John Day Formation and Columbia River Basalt, and Columbia River Basalt and Dalles Formation.\r\n\r\nThe John Day Formation, the only unit studied in detail, consists of about 4,000 feet of tuff, lapilli tuff, strongly to weakly welded rhyolite ash flows, and less abundant trachyandesite flows and rhyolite flows and domes. The formation was divided into nine mappable members in part of the area, primarily on the basis of distinctive ledge-forming welded ash-flow sheets. Most of the sheets are composed of stony rhyolite containing abundant lithophysae and sparse phenocrysts. One sheet contains 10 to 20 percent phenocrysts, mostly cryptoperthitic soda sanidine, but including less abundant quartz, myrmekitic intergrowths of quartz and sanidine, and oligoclase. The rhyolitic ash flows and lava flows were extruded from nearby vents, in contrast to some of the interbedded air-fall tuff and lapilli tuff of dacitic and andesitic composition that may have been derived from vents in an ancestral Cascade Range. The John Day is dated on the basis of a late Oligocene flora near the base of the formation and early Miocene faunas near the top of the formation.\r\n\r\nThe middle Miocene and older rocks in the Antelope-Ashwood area are broadly folded and broken along northeast-trending faults. Over much of the area the rocks dip gently eastward from the crest of a major fold and are broken along a series of steeply dipping antithetic strike faults. Pliocene and Quaternary strata appear to be undeformed.\r\n\r\nAt the Priday agate deposit, chalcedony-filled spherulites (thunder-eggs) occur in the lower part of a weakly welded rhyolitic ash flow. The so-called thunder-eggs are small spheroidal bodies, about 3 inches in average diameter; each consists of a chalcedonic core surrounded by a shell of welded tuff that is altered to radially oriented fibers of cristobalite and alkalic feldspar.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to general geology (Bulletin 1161)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1161D","collaboration":"Prepared in cooperation with the State of Oregon, Department of Geology ande Mineral Industries","usgsCitation":"Peck, D.L., 1964, Geologic reconnaissance of the Antelope-Ashwood area, north-central Oregon, with emphasis on the John Day Formation of late Oligocene and early Miocene age: U.S. Geological Survey Bulletin 1161, Report: iii, 26 p.; 1 Plate: 31.50 × 13.00 inches, https://doi.org/10.3133/b1161D.","productDescription":"Report: iii, 26 p.; 1 Plate: 31.50 × 13.00 inches","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":63365,"rank":399,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1161d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":109435,"rank":699,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20913.htm","linkFileType":{"id":5,"text":"html"},"description":"20913"},{"id":63366,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1161d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":166225,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1161d/report-thumb.jpg"}],"country":"United States","state":"Oregon","otherGeospatial":"Antelope-Ashwood area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121,\n 44.5\n ],\n [\n -120.449,\n 44.5\n ],\n [\n -120.449,\n 45\n ],\n [\n -121,\n 45\n ],\n [\n -121,\n 44.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a83d6","contributors":{"authors":[{"text":"Peck, Dallas L.","contributorId":60187,"corporation":false,"usgs":true,"family":"Peck","given":"Dallas","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":214693,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1258,"text":"wsp1618 - 1964 - Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1618","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1618","title":"Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California","docAbstract":"The San Joaquin Valley includes roughly the southern two-thirds of the Central Valley of California, extending 250 miles from Stockton on the north to Grapevine at the foot of the Tehachapi Mountains. The valley floor ranges in width from 25 miles near Bakersfield to about 55 miles near Visalia; it has a surface area of about 10,000 square miles. More than one-quarter of all the ground water pumped for irrigation in the United States is used in this highly productive valley. Withdrawal of ground water from storage by heavy pumping not only provides a needed irrigation water supply, but it also lowers the ground-water level and makes storage space available in which to conserve excess water during periods of heavy runoff. A storage capacity estimated to be 93 million acre-feet to a depth of 200 feet is available in this ground-water reservoir. This is about nine times the combined capacity of the existing and proposed surface-water reservoirs in the San Joaquin Valley under the California Water Plan.\r\n\r\nThe landforms of the San Joaquin Valley include dissected uplands, low plains and fans, river flood plains and channels, and overflow lands and lake bottoms. Below the land surface, unconsolidated sediments derived from the surrounding mountain highlands extend downward for hundreds of feet. These unconsolidated deposits, consisting chiefly of alluvial deposits, but including some widespread lacustrine sediments, are the principal source of ground water in the valley. Ground water occurs under confined and unconfined conditions in the San Joaquin Valley. In much of the western, central, and southeastern parts of the valley, three distinct ground-water reservoirs are present. In downward succession these are 1) a body of unconfined and semiconfined fresh water in alluvial deposits of Recent, Pleistocene, and possibly later Pliocene age, overlying the Corcoran clay member of the Tulare formation; 2) a body of fresh water confined beneath the Corcoran clay member, which occurs in alluvial and lacustrine deposits of late Pliocene age or older; and 3) a body of saline connate water contained in marine sediments of middle Pliocene or older age, which underlies the fresh-water body throughout the area. In much of the eastern part of the valley, especially in the areas of the major streams, the Corcoran clay member is not present and ground water occurs as one fresh-water body to considerable depth.\r\n\r\nThe ground-water body is replenished by infiltration of rainfall, by infiltration from streams, canals, and ditches, by underflow entering the valley from tributary stream canyons, and by infiltration of excess irrigation water. In much of the valley, however, the annual rainfall is so low that little penetrates deeply, and soil-moisture deficiency is perennial. Infiltration from stream channels and canals and from irrigated fields are the principal sources of groundwater recharge. The ground-water storage capacity of the San Joaquin Valley has been estimated in an earlier report (Davis and others, 1959) as 93 million acre-feet. This is the quantity of water that would drain by gravity from the valley deposits if the regional water level were lowered from 10 to 200 feet below the land surface. Storage capacity was estimated for only the part of the valley considered to be potentially usable as a ground-water reservoir. In this study, a 200foot depth was selected as a practical valley-wide depth limit for unwatering \r\n\r\nunder full utilization of the ground-water reservoir, even though in localized areas sections in excess of 350 feet in depth have already been dewatered. Some of the factors that locally limit the utilization of the ground-water reservoir are inferior water quality, relatively impermeable surface soils, and relatively impermeable subsurface deposits. On the basis of a detailed analysis of la peg model, the subsurface geology of the San Joaquin Valley was subdivided into predominantly permeable and impermeable zones in the 1","language":"ENGLISH","publisher":"United States Govt. Print. Off.,","doi":"10.3133/wsp1618","usgsCitation":"Davis, G.H., Lofgren, B.E., and Mack, S., 1964, Use of ground-water reservoirs for storage of surface water in the San Joaquin Valley, California: U.S. Geological Survey Water Supply Paper 1618, vii, 125 p. :illus., maps, diagrs., tables. and portfolio ;24 cm., https://doi.org/10.3133/wsp1618.","productDescription":"vii, 125 p. :illus., maps, diagrs., tables. and portfolio ;24 cm.","costCenters":[],"links":[{"id":137412,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1618/report-thumb.jpg"},{"id":26195,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26196,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26197,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26198,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26199,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26200,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26201,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26202,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26203,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26204,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26205,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1618/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26206,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1618/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604592","contributors":{"authors":[{"text":"Davis, G. H.","contributorId":40963,"corporation":false,"usgs":true,"family":"Davis","given":"G.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143449,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lofgren, B. E.","contributorId":42579,"corporation":false,"usgs":true,"family":"Lofgren","given":"B.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":143450,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mack, Seymour","contributorId":101247,"corporation":false,"usgs":true,"family":"Mack","given":"Seymour","email":"","affiliations":[],"preferred":false,"id":143451,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1023,"text":"wsp1669U - 1964 - Ground-water resources of Waupaca County, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-02T13:05:28","indexId":"wsp1669U","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":"1669","chapter":"U","title":"Ground-water resources of Waupaca County, Wisconsin","docAbstract":"Waupaca County is in east-central Wisconsin. No serious ground-water problems existed in 1960 except in a few localities where crystalline rock is near land surface or is covered by nearly impermeable till. The use of ground water for irrigation has not appreciably affected ground-water levels.
\nThe county is covered by Pleistocene till, glaciolacustrine (lake), glaciofluvial (stream), and eolian (wind) deposits. In the northern three-quarters of the county these deposits overlie Precambrian crystalline rocks; in the remainder, they overlie sandstone of Cambrian age and, to a minor extent, dolomite of the Prairie du Chien Group of Ordovician age. The deposits of Pleistocene age, particularly outwash, are the principal sources of ground water except in those areas where the saturated thickness is slight or the permeability low. The sandstone of Cambrian age is an important aquifer in the southeastern part of the county. The crystalline rocks of Precambrian age yield little water except from fractures, joints, and weathered zones, and they are a source of water only in areas where better aquifers are absent.
\nGround water in Waupaca County occurs under both water-table and artesian conditions. The source of this ground water is precipitation that falls on the county and percolates downward to the zone of saturation. Regional movement of ground water is to the Wolf River. In most of the county the direction of movement is eastward or southeastward, except in the southeastern corner of the county, where the movement is westward.
\nWater-level fluctuations reflect the variations of ground-water storage or artesian pressure in response to variations in recharge and discharge. Declining water levels from 1956 to 1959 reflect a period of below-normal precipitation, and rising water levels in late 1959 and 1960 reflect above-normal precipitation. Average precipitation, runoff, and evapotranspiration in 1959 are estimated to be 1,000, 400, and 600 mgd (million gallons per day) respectively. Pumpage in the county was estimated to be about 4 mgd in 1959, and about half of this amount was used for public supplies.
\nA pumping test of a well in outwash deposits near Waupaca indicated that at that point the coefficient of transmissibility is about 100,000 gpd (gallons per day) per ft, the permeability is about 1,000 gpd per sq ft, the coefficient of storage is about 0.2, and the specific capacity is 41 gpm (gallons per minute) per ft of drawdown. These hydraulic characteristics are probably in the same order of magnitude as the characteristics of outwash deposits in the county in general.
\nThe water from wells in Waupaca County, although hard and generally containing iron, is good for most purposes.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States, 1962","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1669U","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey, University of Wisconsin","usgsCitation":"Berkstresser, C., 1964, Ground-water resources of Waupaca County, Wisconsin: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 38 p.; 7 Plates: 32.00 x 34.06 inches or smaller, https://doi.org/10.3133/wsp1669U.","productDescription":"Report: iv, 38 p.; 7 Plates: 32.00 x 34.06 inches or smaller","numberOfPages":"42","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":137935,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669u/report-thumb.jpg"},{"id":25641,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25642,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25643,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25644,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25645,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25646,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25647,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669u/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25648,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669u/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","county":"Waupaca County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-88.6062,44.5903],[-88.6152,44.5903],[-88.7371,44.5906],[-88.7368,44.5021],[-88.7365,44.4164],[-88.7381,44.3307],[-88.7397,44.2432],[-88.7658,44.2434],[-88.8609,44.2425],[-88.8871,44.2426],[-88.9821,44.243],[-89.007,44.2426],[-89.104,44.243],[-89.1288,44.243],[-89.2245,44.2433],[-89.2242,44.3308],[-89.2238,44.4174],[-89.2235,44.504],[-89.2231,44.5916],[-89.2234,44.6814],[-88.982,44.6798],[-88.8587,44.6797],[-88.7367,44.6791],[-88.6051,44.6783],[-88.6062,44.5903]]]},\"properties\":{\"name\":\"Waupaca\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d523","contributors":{"authors":[{"text":"Berkstresser, Charles F.","contributorId":33697,"corporation":false,"usgs":true,"family":"Berkstresser","given":"Charles F.","affiliations":[],"preferred":false,"id":143042,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"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":2796,"text":"wsp1608D - 1964 - Artesian water in the Malabar coastal plain of southern Kerala, India","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1608D","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":"D","title":"Artesian water in the Malabar coastal plain of southern Kerala, India","docAbstract":"The present report is based on a geological and hydrological reconnaissance during 1954 of the Malabar Coastal Plain and adjacent island area of southern Kerala to evaluate the availability of ground water for coastal villages and municipalities and associated industries and the potentialities for future development. The work was done in cooperation with the Geological Survey of India and under the auspices of the U.S. Technical Cooperation Mission to India. The State of Kerala, which lies near the southern tip of India and along the eastern shore of the Caspian Sea, contains a total area of 14,937 square miles. The eastern part of the state is s rugged mountainous highland which attains \r\naltitudes of more than 6,000 feet. This highland descends westward through piedmont upland to s narrow coastal plain, which reaches a maximum width of about 16 miles in the latitude of Shertalli. A tropical monsoon rain-forest climate prevails in most of Kerala, and annual rainfall ranges from 65 to 130 inches in the southern part of the coastal plain to as much a 200 inches in the highland. \r\n\r\nThe highland and piedmont upland tracts of Kerala are underlain by Precambrian meamorphic and igneous rocks belonging in large parabola-the so-called Charnockite Series. Beneath ahe coastal plain are semiconsolidated asunconsolidated sedimentary deposits whose age ranges from Miocene to Recent. These deposits include sofa sandstone and clay shale containing some marl or limestone and sand, and clay and pea containing some gravel. The sofa sandstone, sand, and gravel beds constitute important aquifers a depths ranging from a few tens of feet to 400 feet or more below the land surface. The shallow ground war is under water-able or unconfined conditions, but the deeper aquifers contain water under artesian pressure. Near the coast, drilled wells tapping the deeper aquifers commonly flow with artesian heads as much as 10 to 12 feet above the land surface. \r\n\r\nThe draft from existing wells in the coastal belt between Quilon and Alleppy was estimated at 1 to 1 1/2 million imperial gallons a day. However, favorable conations exist for considerable further ground-water development in the coastal plain provided that sufficient attention is given to the potential hazards of saltwater encroachment and local overdevelopment. It is estimated that the overall potential for development of water from wells is probably at least several tens of millions of gallons a day, and perhaps more, in the Malabar Coastal Plain of southern Kera. Such a draft would have to be well dispersed to avoid overdevelopment and salt-war encroachment.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608D","usgsCitation":"Taylor, G., and Ghosh, P., 1964, Artesian water in the Malabar coastal plain of southern Kerala, India: U.S. Geological Survey Water Supply Paper 1608, iii, 14 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1608D.","productDescription":"iii, 14 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138615,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608d/report-thumb.jpg"},{"id":29292,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29293,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29294,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672c6d","contributors":{"authors":[{"text":"Taylor, George C.","contributorId":45693,"corporation":false,"usgs":true,"family":"Taylor","given":"George C.","affiliations":[],"preferred":false,"id":145806,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ghosh, P.K.","contributorId":53771,"corporation":false,"usgs":true,"family":"Ghosh","given":"P.K.","email":"","affiliations":[],"preferred":false,"id":145807,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2043,"text":"wsp1669J - 1964 - Ground-water conditions in the Green Bay area, Wisconsin, 1950-60","interactions":[],"lastModifiedDate":"2015-10-02T13:57:06","indexId":"wsp1669J","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":"1669","chapter":"J","title":"Ground-water conditions in the Green Bay area, Wisconsin, 1950-60","docAbstract":"The Green Bay area, which includes parts of Brown, Outagamie, and Shawano Counties, has an area of about 525 square miles in eastern Wisconsin at the south end of Green Bay. In 1960, it had a population estimated at 124,000; Green Bay, the largest city in the area, had a population of 62,888. The Green Bay area is underlain by a basement complex of crystalline rocks of Precambrian age. Sedimentary rocks of Cambrian, Ordovician, and Silurian ages overlie the crystalline rocks. These rocks are divided, in ascending order, as follows: The Dresbach Group, Franconia Sandstone, and Trempealeau Formation of Cambrian age; the Prairie du Chien Group, St. Peter Sandstone, Platteville Formation, and Maquoketa Shale of Ordovician age; and the Niagara Dolomite of Silurian age. The Maquoketa Shale and Niagara Dolomite are present only in the eastern part of the area. Unconsolidated deposits, largely of Pleistocene age and glacial origin, overlie the older rocks in most of the area. The rocks of the Dresbach Group, Franconia Sandstone, Trempealeau Formation, Prairie du Chien Group, and St. Peter Sandstone are connected hydraulically and can be considered to form one aquifer, called the sandstone aquifer. The sandstone aquifer is the principal source of ground-water supply in the Green Bay area and is one of the most productive water-bearing units in Wisconsin. All the public water supplies in the area, except the supply for the city of Green Bay, and many of the industrial water supplies are obtained from wells tapping the sandstone aquifer. Rates of discharge of individual wells range from about 200 to 1,000 gallous per minute. The city of Green Bay also obtained its water supply from wells tapping the sandstone aquifer until August 1957, when it began using Lake Michigan as a source of water supply. Several industries also use large quantities of surface water. The Niagara Dolomite, although largely undeveloped, is potentially an important aquifer, in the eastern part of the area. Small amounts of water are obtained from dolomite of the Platteville Formation and from sand and gravel deposits of Pleistocene age. Recharge to the sandstone aquifer in the Green Bay area is derived chiefly from precipitation that infiltrates at or near the outcrop area of the aquifer in northwestern Brown County, eastern Outagamie and Shawano Counties, and southern Oconto County. The amount of recharge is estimated to be at least 30 mgd (million gallons per day). Withdrawals of water from wells tapping the sandstone aquifer in the area began when the first well was drilled in 1886. The withdrawals gradually increased to an average of about 6 mgd in 1940, about 10 mgd in 1950, and about 13 mgd in January-July of 1957, after which time the city of Green Bay discontinued pumping from wells. From August 1957 through 1960, average annual withdrawals of water remained relatively constant at about 5 mgd. Water levels in wells tapping the sandstone aquifer persistently declined until August 1957 as a result of the gradually increasing withdrawals of water. In the area of concentrated ground-water withdrawals in downtown Green Bay, the piezometric surface, which had been about 100 feet above land surface in 1886, was about 340 feet below land surface in 1957. The cessation of pumping by the city of Green Bay in August 1957 resulted in a decrease in withdrawals of ground water from about 13.1 mgd in the first half of 1957 to about 5.3 mgd in the last half and a rapid recovery in water levels. ]n the area of concentrated withdrawals, the piezometric surface had recovered about 300 feet by September 1960. Rises in water levels were recorded throughout the Green Bay area, with the amount of the rise depending on the distance from the Green Bay city wells. In September 1960, water levels appeared to be affected more by local variations in the rates of pumping than by the recovery resulting from 1957 reduction in pumping. Much additional ground water could
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1669J","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey","usgsCitation":"Knowles, D., 1964, Ground-water conditions in the Green Bay area, Wisconsin, 1950-60: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 37 p.; 6 Plates: 20.00 x 33.40 inches or smaller, https://doi.org/10.3133/wsp1669J.","productDescription":"Report: iv, 37 p.; 6 Plates: 20.00 x 33.40 inches or smaller","numberOfPages":"37","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":137710,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669j/report-thumb.jpg"},{"id":27532,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27533,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27534,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27535,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27536,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27537,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669j/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27538,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669j/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wisconsin","otherGeospatial":"Green Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.28475952148438,\n 44.21075694234126\n ],\n [\n -88.28475952148438,\n 44.71161010858431\n ],\n [\n -87.82058715820312,\n 44.71161010858431\n ],\n [\n -87.82058715820312,\n 44.21075694234126\n ],\n [\n -88.28475952148438,\n 44.21075694234126\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66d218","contributors":{"authors":[{"text":"Knowles, Doyle B.","contributorId":85566,"corporation":false,"usgs":true,"family":"Knowles","given":"Doyle B.","affiliations":[],"preferred":false,"id":144579,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13574,"text":"ofr6453 - 1964 - Subsurface geology of the upper Cretaceous Kirtland and Fruitland formations of the San Juan Basin, New Mexico and Colorado","interactions":[],"lastModifiedDate":"2025-06-12T20:14:48.500091","indexId":"ofr6453","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":"64-53","title":"Subsurface geology of the upper Cretaceous Kirtland and Fruitland formations of the San Juan Basin, New Mexico and Colorado","docAbstract":"The San Juan Basin is an asymmetrical structural basin in northwestern New Mexico and southwestern Colorado. The basin contains sedimentary rocks ranging from Cambrian through Recent in age and attaining a maximum thickness between 14,000 and 15,000 feet. The Upper Cretaceous sedimentary rocks exceed 8,000 feet in thickness and can be divided into two groups: the lower Upper Cretaceous which is composed of the non marine and non-marine rocks and the upper Upper Cretaceous which is composed of the non-marine Kirtland and Fruitland Formations. The Kirtland Shale is subdivided into the lower shale, Farmington Sandstone, and upper shale members.
The rocks of the Kirtland and Fruitland Formations consist of fluviatile and flood plain deposits and range in thickness from 1750 feet in the northwest part of the basin to 0 feet on the eastside of the basin. The thinning of the Kirtland and Fruitland Formations from west to east is primarily the result of erosion following tilting of the San Juan Basin area toward the west after either part or all of the upper shale member had been deposited. The overlying Ojo Alamo Sandstone rests on progressively older rocks across the basin overstepping the under lying upper shale member, Farmington Sandstone Member, Fruitland Formation, and finally resting on the Lewis Shale on the east side of the basin. The source area for the rocks of the Kirtland and Fruitland Formations was probably to the north or northwest of the San Juan Basin area.
The Kirtland and Fruitland rocks have produced minor amounts of oil and gas. The Fruitland Formation contains large coal deposits some of which are currently being strip mined near Fruitland, New Mexico
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6453","usgsCitation":"Fassett, J.E., 1964, Subsurface geology of the upper Cretaceous Kirtland and Fruitland formations of the San Juan Basin, New Mexico and Colorado: U.S. Geological Survey Open-File Report 64-53, Report: 93 p.; 12 Plates: 48.29 x 25.08 inches or smaller, https://doi.org/10.3133/ofr6453.","productDescription":"Report: 93 p.; 12 Plates: 48.29 x 25.08 inches or smaller","costCenters":[],"links":[{"id":490599,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490600,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490601,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490602,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490603,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490604,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490605,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490606,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490607,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490608,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490609,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147205,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0053/report-thumb.jpg"},{"id":490597,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0053/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490598,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1964/0053/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Colorado, New Mexico","otherGeospatial":"San Juan Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -109.95401765016268,\n 41.257729787434215\n ],\n [\n -109.95401765016268,\n 31.151066456218246\n ],\n [\n -101.92656228630202,\n 31.151066456218246\n ],\n [\n -101.92656228630202,\n 41.257729787434215\n ],\n [\n -109.95401765016268,\n 41.257729787434215\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699a33","contributors":{"authors":[{"text":"Fassett, James E. jfassett@usgs.gov","contributorId":73590,"corporation":false,"usgs":true,"family":"Fassett","given":"James","email":"jfassett@usgs.gov","middleInitial":"E.","affiliations":[{"id":165,"text":"Central Energy Resources Team","active":false,"usgs":true}],"preferred":false,"id":168045,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1989,"text":"wsp1776 - 1964 - Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water","interactions":[{"subject":{"id":52182,"text":"ofr6179 - 1961 - Basic data, ground-water resources and geology of Washington, D. C., and vicinity","indexId":"ofr6179","publicationYear":"1961","noYear":false,"title":"Basic data, ground-water resources and geology of Washington, D. C., and vicinity"},"predicate":"SUPERSEDED_BY","object":{"id":1989,"text":"wsp1776 - 1964 - Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water","indexId":"wsp1776","publicationYear":"1964","noYear":false,"title":"Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water"},"id":1}],"lastModifiedDate":"2023-11-02T21:05:20.22677","indexId":"wsp1776","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":"1776","title":"Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water","docAbstract":"The area of this report includes 436 square miles centered about the District of Columbia.
The area contains parts of two distinctly different physiographic provinces-the Piedmont and the Coastal Plain. The Fall Line, which separates the Piedmont province on the west from the Coastal Plain Province on the east, bisects the area diagonally from northeast to southwest. Northwest of the Fall Line, deeply weathered igneous and metamorphic rocks are exposed ; to the southeast, these rocks are covered by Coastal Plain sediments; the nonconformity between crystalline rock and sediments dips southeast at an average rate of about 125 feet per mile.
The rocks of the Piedmont include: (1) schist, phyllite, and quartzite of the Wissahickon Formation; (2) altered mafic rocks such as greenstone and serpentine; (3) the Laurel Gneiss of Chapman, 1942, and the Sykesville Formation of Jonas, 1928--both probably derived from the Wissahickon ; and (4) later granitic intrusive rocks.
Lying upon this basement of hard rocks east of the Fall Line are the generally unconsolidated sediments of the Coastal Plain, which include gravel, sand, and clay, ranging in age from Cretaceous to Recent. These sediments measure only a few inches at their western extremity but thicken to 1,800 feet at the southeast corner of the mapped area.
Owing to the great diversity in the geology of the two provinces, the waterbearing characteristics of the rocks also vary greatly. In the Piedmont, ground water occurs under unconfined or water-table conditions in openings and fissures in the hard rocks or in the residual weathered blanket that overlies them. In the Coastal Plain, the shallow wells tap unconfined water, but beneath the upper clay layers the water is contained in the sand and gravel under artesian pressure and must be recovered by deep drilled wells.
Wells are of three types--drilled, bored, and dug. Drilled wells furnish a permanent water supply and are the least subject to pollution when properly constructed. Bored or dug wells allow greater storage capacity and are satisfactory for domestic supplies in some locations, but they are polluted easily. If not properly constructed or of sufficient depth, they may fail in dry weather.
Ground-water supplies for domestic use, 5 to 10 gpm (gallons per minute), are obtainable in most places. In the Piedmont, recorded yields in drilled wells range from 0.2 to 212 gpm. In the Coastal Plain, wells yield from 1 to 800 gpm.
The quality of the ground water in the report area is generally satisfactory for domestic, industrial, and irrigation use. High iron content and corrosiveness are troublesome in places. The water is soft to moderately hard--2 to 175 ppm (parts per million). Water in the Piedmont province is. dominantly the calcium and bicarbonate type; in the Coastal Plain most water is of calcium-magnesium bicarbonate type.
In the Piedmont, careful location of wells with respect to the geology (rock type and structure) and to topography usually results in higher yields and may mean the difference between success and failure. In the Coastal Plain, drilled artesian wells are not affected by topography, but the yield obtained depends upon the penetration of a water-bearing sand or gravel bed at sufficient depth.
The early settlers obtained water from the springs and streams, and later from dug wells. After Washington was established as the Capital in 1800, water was obtained from public and privately owned wells. Water was piped from some of the springs to government buildings and to private homes and business houses. In 1863 a diversion dam was completed in the Potomac above Great Falls and a conduit was built into the city to furnish a public water supply. This system with modifications has been in use ever since. A new diversion dam and pumping station at Little Falls was put into service in the summer of 1959.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1776","usgsCitation":"Johnston, P.M., Weaver, D.E., and Siu, L., 1964, Geology and ground-water resources of Washington, D.C., and vicinity, with a section on chemical quality of the water: U.S. Geological Survey Water Supply Paper 1776, Report: vi, 97 p.; 2 Plates: 34.50 x 26.60 inches and 21.00 x 28.60 inches, https://doi.org/10.3133/wsp1776.","productDescription":"Report: vi, 97 p.; 2 Plates: 34.50 x 26.60 inches and 21.00 x 28.60 inches","costCenters":[],"links":[{"id":422360,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_16352.htm","linkFileType":{"id":5,"text":"html"}},{"id":27381,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1776/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27382,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1776/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138471,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1776/report-thumb.jpg"},{"id":27380,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1776/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"District of Columbia","city":"Washington D.C.","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-77.038598,38.791513],[-77.038898,38.800813],[-77.035798,38.814913],[-77.038098,38.815613],[-77.039098,38.821413],[-77.038098,38.828612],[-77.039199,38.832212],[-77.041199,38.833712],[-77.042599,38.833812],[-77.043499,38.833212],[-77.044899,38.834712],[-77.044999,38.838512],[-77.044489,38.839595],[-77.044199,38.840212],[-77.041699,38.840212],[-77.032798,38.841712],[-77.031698,38.850512],[-77.039299,38.864312],[-77.038899,38.865812],[-77.039099,38.868112],[-77.040599,38.871212],[-77.043299,38.874012],[-77.045399,38.875212],[-77.046599,38.874912],[-77.045599,38.873012],[-77.046299,38.871312],[-77.049099,38.870712],[-77.051299,38.873212],[-77.051099,38.875212],[-77.054099,38.879112],[-77.055199,38.880012],[-77.058254,38.880069],[-77.063499,38.888611],[-77.067299,38.899211],[-77.068199,38.899811],[-77.070099,38.900711],[-77.0822,38.901911],[-77.0902,38.904211],[-77.0937,38.905911],[-77.1012,38.911111],[-77.1034,38.912911],[-77.1063,38.919111],[-77.1134,38.925211],[-77.1166,38.928911],[-77.1179,38.932411],[-77.119857,38.93427],[-77.1199,38.934311],[-77.1045,38.94641],[-77.1007,38.94891],[-77.0915,38.95651],[-77.054299,38.98511],[-77.040999,38.99511],[-77.036299,38.99171],[-77.015598,38.97591],[-77.013798,38.97441],[-77.008298,38.97011],[-77.002636,38.965521],[-77.002498,38.96541],[-76.941519,38.918276],[-76.935096,38.913311],[-76.909395,38.892812],[-76.910795,38.891712],[-76.919295,38.885112],[-76.920195,38.884412],[-76.949696,38.861312],[-76.953696,38.858512],[-76.979497,38.837812],[-76.992697,38.828213],[-76.999997,38.821913],[-77.001397,38.821513],[-77.024392,38.80297],[-77.038598,38.791513]]]},\"properties\":{\"name\":\"District of Columbia\",\"nation\":\"USA \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685810","contributors":{"authors":[{"text":"Johnston, Paul McKelvey","contributorId":8828,"corporation":false,"usgs":true,"family":"Johnston","given":"Paul","email":"","middleInitial":"McKelvey","affiliations":[],"preferred":false,"id":144482,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weaver, D. E.","contributorId":51718,"corporation":false,"usgs":true,"family":"Weaver","given":"D.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":887473,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Siu, Leonard","contributorId":331349,"corporation":false,"usgs":false,"family":"Siu","given":"Leonard","email":"","affiliations":[],"preferred":false,"id":887474,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":3221,"text":"cir489 - 1964 - A magnetic anomaly of possible economic significance in southeastern Minnesota","interactions":[],"lastModifiedDate":"2018-01-02T19:49:02","indexId":"cir489","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":"489","title":"A magnetic anomaly of possible economic significance in southeastern Minnesota","docAbstract":"An aeromagnetic survey in southeastern Minnesota by the U. S. Geological Survey in cooperation with the State of Minnesota has revealed a high-amplitude, linear, and narrow magnetic feature that suggests a possible source of Precambrian iron-formation of economic value. \r\n\r\nFor the past few years the U. S. Geological Survey has been conducting detailed geophysical studies of the midcontinent gravity anomaly--a broad, high-amplitude feature that extends from Lake Superior through the States of Minnesota, Iowa, Nebraska, and part of Kansas. As part of this study an aeromagnetic survey of the southern part of the State was made in cooperation with the State of Minnesota during the summer of 1963, in which a linear high-amplitude anomaly of the order of 4,000 gammas was discovered. Because of the high amplitude, the linearity, and the narrowness of the magnetic feature, it is believed the source may be Precambrian iron-formation of possible economic value. \r\n\r\nThe anomalous area is in Fillmore County, approximately between the towns of Lanesboro and Peterson in the extreme southeastern part of the State. (See figures 1 and 2.) At the site of the anomaly, Cambrian sedimentary rocks occur in the valley of the Root River, and Ordovician rocks (nearly flat lying) mantle the upland areas. \r\n\r\nThe uplands are largely covered by glacial deposits, which are relatively thin (Paul K. Sims, written communication, 1964). Depths to the Precambrian are estimated to range from 500 feet to 1,000 feet below the surface. \r\n\r\nThe aeromagnetic map shown in figure 2 was compiled from continuous magnetic profiles made along east-west flight lines 1,000 feet above ground, and spaced approximately 1 mile apart. Contour intervals of 20, 100, and 500 gammas were used depending on the intensity. The instrument for the survey was a flux-gate type magnetometer (AN/ASQ-3A) which measures total-field variations. The contour map displays variations in magnetic pattern which are typical of shallow Precambrian rocks. Anomalies of the order of 1,000 gammas are shown along the east and west edges of the map. The outstanding feature is the previously mentioned linear positive anomaly that trends northeast and reaches a peak of 3,960 gammas. The positive anomaly is contoured from data on four consecutive profiles, but only two show high amplitudes. The high-amplitude anomalies along traverses 1 and 2 are shown in figure 3. \r\n\r\nDepth calculations suggest that the source of the anomaly lies about 1,000 feet below the surface. Assuming a dikelike source and magnetization resulting entirely from induction in the earth's field, several calculations were made in an attempt to fit the magnetic profile taken along the line AA' (see figs. 2 and 4), considered to be a typical cross-section of the magnetic anomaly. Comparisons are shown between observed and computed profiles. The fixed parameters used were (a) distance from detector to source of 2,000 ft; width of dike of 5,000 ft; dip of dike of 75?, 90?, 105? , and 120? , as shown. The best fit occurs when the dike is vertical or dips 75? to the southwest. For these cases, the susceptibility, k, is computed to be 0.016 c.g.s, units, and is comparable to k = 0.02+ calculated by Bath (1962) for the relatively unmetamorphosed iron-formation of the Main Megabi district in Minnesota where the induced magnetization was most likely the dominant magnetization. If the dominant magnetization for the anomaly in Fillmore County were remanent rather than induced, the economic importance of the anomaly would be greatly reduced. \r\n\r\nThis anomaly seems sufficiently promising to warrant further geologic and geophysical investigation. Detailed ground magnetic and electrical studies would be useful to delineate the feature. In the final analysis, however, the presence of iron-formation can be determined only by the drill.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir489","usgsCitation":"Zietz, I., 1964, A magnetic anomaly of possible economic significance in southeastern Minnesota: U.S. Geological Survey Circular 489, 5 p. :maps ;27 cm., https://doi.org/10.3133/cir489.","productDescription":"5 p. :maps ;27 cm.","costCenters":[],"links":[{"id":138944,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1964/0489/report-thumb.jpg"},{"id":30214,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1964/0489/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ae1de","contributors":{"authors":[{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":146462,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2797,"text":"wsp1608B - 1964 - Ground water in folded Cretaceous sandstone of the Bhachau area, Kutch, India, with reference to the Kandla Port water supply","interactions":[],"lastModifiedDate":"2012-02-02T00:05:28","indexId":"wsp1608B","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":"B","title":"Ground water in folded Cretaceous sandstone of the Bhachau area, Kutch, India, with reference to the Kandla Port water supply","docAbstract":"This report is based on an investigation of the availability of ground-water supplies in the Bhachau area for the nearby Kandla Port and township development undertaken by the Government of India. This seaport lies on an estuary of the Gulf of Kutch in western India and in the eastern part of the State of Kutch. The fieldwork on the investigation was carried on from November 1952 through April 1953 with continuing hydrologic observations through 1954-55. The fieldwork included: geologic mapping and delimitation of the principal aquifers of the region; preparation of water-table maps; a detailed inventory of existing wells and springs; observations of significant water table fluctuations; preparation of isobicarb, isochlor and isosulf maps to show the areal distribution of ground-water salinity. \r\n\r\nThe Bhachau area includes about 116 square miles in eastern Kutch and lies in a belt of semiarid low-latitude steppes. The mean annual rainfall is about 15 inches, most of which falls from late June to late September during the southwest monsoon. The area includes a central sandy upland ranging from about 100 to 250 feet above sea level ; a northern lowland of between about 50 to 125 feet altitude that slopes north to the Great Rann of Kutch; a belt of low buttes and discontinuous ridges ranging from about 200 to 275 feet above sea level; and southern lowland which slopes in a southerly to southeasterly direction from an altitude of about 125 feet to 25 feet or less near the Gulf of Kutch. The principal streams are Kageshwar Vokra and Kara Vokra which drain north to the Great Rann and Kotwala Vokra and Dalwala Vokra which drain south toward the Gulf of Kutch. \r\n\r\nThe rocks of the Bhachau area include nonmarine and marine sediments of Mesozoic, Tertiary, and Quaternary age and volcanic rocks of late Mesozoic to early Tertiary age. The oldest rocks in the area are medium- to coarse-grained white to buff current-bedded friable sandstone with occasional partings of white silty shale of the Upper Bhuj series that has been assigned to the Early Cretaceous. The soft friable sandstone of the Upper Bhuj series constitutes the most productive ground-water reservoir in the Bhachau area. At present (1955) there are nine irrigated tracts for which water is obtained from dug wells less than 90 feet deep in the Upper Bhuj. These wells are worked by bullocks and 'motes' (leather bags) at withdrawal rates ranging from about 6,000 to 24,000imperial gallons per day; however, many existing individual wells if equipped with mechanical pumps are capable of yielding 100,000 gallons per day. The Deccan trap of Late Cretaceous to Eocene age occurs in a sequence of basaltic lava flows in the Bhachau area, but trap dikes, sills and plugs that are common in other parts of Kutch have not been observed in the area. Laterite of probable Eocene age is extensive at the top of the Deccan trap, and in places where the lava flows are thin the parent rock has been almost completely lateritized. The Deccan lava flows or the laterite, where the trap is absent, rest disconformably on the Upper Bhuj. No wells have been observed in the Deccan trap of the Bhachau area, but it is possible that locally small supplies of good water may be obtained from these rocks. \r\n\r\nThe Tertiary sediments, which are assigned to the Manchhar series of Pliocene age, generally rest on the laterite or the Deccan trap ; but where both are absent, the Manchhar rests directly on the Upper Bhuj. The Manchhar series includes massive reddish-brown gypseous clay shales, laminated gray siltstones, some limestone, mottled sandstone, and laterite trap gravel. Only meager supplies of brackish water are obtained from wells in these sediments. \r\n\r\nAlong the channels of Kotwala, Dalwala, Kageshwar, and Kara Vokras are narrow bands of unconsolidated coarse sand with fine gravel of Quaternary age. No wells were observed in these deposits, but it is possible that locally they may contain small supplies of bracki","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608B","usgsCitation":"Taylor, G., Osa, H., Mitra, A., and Sen, B., 1964, Ground water in folded Cretaceous sandstone of the Bhachau area, Kutch, India, with reference to the Kandla Port water supply: U.S. Geological Survey Water Supply Paper 1608, iv, 31 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1608B.","productDescription":"iv, 31 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":138616,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608b/report-thumb.jpg"},{"id":29295,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29296,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29297,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29298,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1608b/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29299,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66da12","contributors":{"authors":[{"text":"Taylor, George C.","contributorId":45693,"corporation":false,"usgs":true,"family":"Taylor","given":"George C.","affiliations":[],"preferred":false,"id":145810,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Osa, H.M.","contributorId":15594,"corporation":false,"usgs":true,"family":"Osa","given":"H.M.","email":"","affiliations":[],"preferred":false,"id":145809,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mitra, A.","contributorId":97077,"corporation":false,"usgs":true,"family":"Mitra","given":"A.","email":"","affiliations":[],"preferred":false,"id":145811,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Sen, B.N.","contributorId":8079,"corporation":false,"usgs":true,"family":"Sen","given":"B.N.","email":"","affiliations":[],"preferred":false,"id":145808,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":1335,"text":"wsp1535J - 1964 - Chemical composition of snow in the northern Sierra Nevada and other areas","interactions":[],"lastModifiedDate":"2017-09-06T17:45:05","indexId":"wsp1535J","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":"1535","chapter":"J","title":"Chemical composition of snow in the northern Sierra Nevada and other areas","docAbstract":"Melting snow provides a large part of the water used throughout the western conterminous United States for agriculture, industry, and domestic supply. It is an active agent in chemical weathering, supplies moisture for forest growth, and sustains fish and wildlife. Despite its importance, virtually nothing has been known of the chemical character of snow in the western mountains until the present study.
Analysis of more than 100 samples, most from the northern Sierra Nevada, but some from Utah, Denver, Colo., and scattered points, shows that melted snow is a dilute solution containing measurable amounts of some or all of the inorganic constituents commonly found in natural water. There are significant regional differences in chemical composition; the progressive increase in calcium content with increasing distance eastward from the west slope of the Sierra Nevada is the most pronounced. The chemical character of individual snowfalls is variable. Some show predominant influence of oceanic salt; others show strong effects of mineralization from continental sources, probably largely dust. Silica and boron were found in about half the samples analyzed for these constituents; precipitation is seldom analyzed for these substances.
Results of the chemical analyses for major constituents in snow samples are summarized in the following table. The median and mean values for individual constituents are derived from 41-78 samples of Sierra Nevada snow, 6-18 samples of Utah snow, and 6-17 samples of Denver, Colo., snow.
The sodium, chloride, and perhaps boron found in snow are probably incorporated in moisture-laden air masses as they move over the Pacific Ocean. Silica, although abundant in the silicate-mineral nuclei found in some snowflakes, may be derived in soluble form largely from dust. Calcium, magnesium, and some bicarbonate are probably added by dust of continental origin. The sources of the other constituents remain unknown.
When snowmelt comes in contact with the lithosphere, the earlier diversity of chemical type largely disappears. The melt water rapidly increases its content of dissolved solids and becomes calcium magnesium bicarbonate in type. Silica, whose concentration increases more than tenfold, shows the largest gain; calcium and bicarbonate contents also increase markedly. Most of the additional mineral matter is from soft and weathered rock; bicarbonate, however, is largely from the soil atmosphere.
Investigators, some reporting as much as a century ago, concentrated attention largely on nitrogen compounds and seldom reported other constituents except chloride and sulfate. The Northern European precipitation-sampling network provides the most comprehensive collection of data on precipitation chemistry, but it does not segregate snow from other forms of precipitation. The present study establishes with confidence the chemical character of snow in the Sierra Nevada, and suggests that the dissolved-solids content of precipitation increases with increasing distance inland from the Pacific Coast.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1535J","usgsCitation":"Feth, J.H., Rogers, S.M., and Roberson, C.E., 1964, Chemical composition of snow in the northern Sierra Nevada and other areas: U.S. Geological Survey Water Supply Paper 1535, Report: iii, 39 p.; Plate: 28.00 x 21.15 inches, https://doi.org/10.3133/wsp1535J.","productDescription":"Report: iii, 39 p.; Plate: 28.00 x 21.15 inches","numberOfPages":"45","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":26389,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1535j/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26390,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1535j/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137406,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1535j/report-thumb.jpg"},{"id":109971,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24719.htm","linkFileType":{"id":5,"text":"html"},"description":"24719"}],"country":"United States","state":"Arizona, California, Colorado, Nevada, Oregon, Utah","city":"Denver","otherGeospatial":"Sierra Nevada","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e3c6a","contributors":{"authors":[{"text":"Feth, John Henry Frederick","contributorId":37310,"corporation":false,"usgs":true,"family":"Feth","given":"John","email":"","middleInitial":"Henry Frederick","affiliations":[],"preferred":false,"id":143582,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rogers, S. M.","contributorId":101637,"corporation":false,"usgs":true,"family":"Rogers","given":"S.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143584,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Roberson, Charles Elmer","contributorId":79451,"corporation":false,"usgs":true,"family":"Roberson","given":"Charles","email":"","middleInitial":"Elmer","affiliations":[],"preferred":false,"id":143583,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":3092,"text":"wsp1941 - 1964 - Quality of surface waters of the United States, 1962, Parts 1 and 2, North Atlantic slope basins and South Atlantic and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:30","indexId":"wsp1941","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":"1941","title":"Quality of surface waters of the United States, 1962, Parts 1 and 2, North Atlantic slope basins and South Atlantic and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1941","usgsCitation":"Love, S.K., 1964, Quality of surface waters of the United States, 1962, Parts 1 and 2, North Atlantic slope basins and South Atlantic and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 1941, xi, 434 p. :ill. ;23 cm., https://doi.org/10.3133/wsp1941.","productDescription":"xi, 434 p. :ill. ;23 cm.","costCenters":[],"links":[{"id":138644,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1941/report-thumb.jpg"},{"id":29974,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1941/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db651ad7","contributors":{"authors":[{"text":"Love, S. K.","contributorId":27419,"corporation":false,"usgs":true,"family":"Love","given":"S.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":146261,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15272,"text":"ofr64122 - 1964 - Geology applied to study of coal mine bumps and mining methods at Sunnyside, Utah","interactions":[],"lastModifiedDate":"2025-06-17T13:45:06.390094","indexId":"ofr64122","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":"64-122","title":"Geology applied to study of coal mine bumps and mining methods at Sunnyside, Utah","docAbstract":"Coal mine bumps are a serious hazard to life and property in the mines of east-central Utah. Research into geologic factors associated with these bumps indicates that the bumps are spatially and genetically related to structural and stratigraphic features. Some bumps are directly related to stress accumulation along faults, either from natural causes or as a result of mining. Frictional properties of bedding planes between coal and roof rock, and between some rock units within the roof, directly affect the deformation of coal ribs, and hence the incidence of bumps. These frictional properties are related to the lithology of the roof rocks as well as to the sedimentary structures within the rocks. Commonly a sequence consisting of 1- 3 ft of carbonaceous siltstone, about 2- 3 ft of rider coal, and several feet of massive siltstone or sandstone overlies the main seam. The sequence causes difficult roof conditions in the mines, difficult mining conditions, and directly or indirectly many bumps.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr64122","usgsCitation":"Osterwald, F.W., and Dunrud, C., 1964, Geology applied to study of coal mine bumps and mining methods at Sunnyside, Utah: U.S. Geological Survey Open-File Report 64-122, 8 p., https://doi.org/10.3133/ofr64122.","productDescription":"8 p.","costCenters":[],"links":[{"id":490818,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1964/0122/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":148173,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0122/report-thumb.jpg"}],"country":"United States","state":"Utah","city":"Sunnyside","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"id\":\"47\",\"properties\":{\"name\":\"Utah\",\"nation\":\"USA 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Frank W.","contributorId":98301,"corporation":false,"usgs":true,"family":"Osterwald","given":"Frank","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":170862,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dunrud, C. Richard","contributorId":48964,"corporation":false,"usgs":true,"family":"Dunrud","given":"C. Richard","affiliations":[],"preferred":false,"id":170861,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2099,"text":"wsp1669AA - 1964 - Ground-water resources of the lower Mesilla Valley, Texas and New Mexico","interactions":[],"lastModifiedDate":"2016-08-19T14:33:03","indexId":"wsp1669AA","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":"1669","chapter":"AA","title":"Ground-water resources of the lower Mesilla Valley, Texas and New Mexico","docAbstract":"The lower Mesilla Valley extends southward from the vicinity of Anthony, Tex., to the gorge of the Rio Grande north of El Paso and westward from the Franklin Mountains to the east edge of La Mesa. The increase in the use of ground water for the public water supply of El Paso and for supplemental irrigation, when the surface-water allotments were inadequate, emphasized the need for an investigation of the ground-water resources of the lower Mesilla Valley.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to the hydrology of the United States, 1962","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1669AA","usgsCitation":"Leggat, E., Lowry, M., and Hood, J.W., 1964, Ground-water resources of the lower Mesilla Valley, Texas and New Mexico: U.S. Geological Survey Water Supply Paper 1669, Report: iv, 49 p.; 8 Plates, https://doi.org/10.3133/wsp1669AA.","productDescription":"Report: iv, 49 p.; 8 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":27666,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27667,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27668,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27669,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27672,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27673,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1669aa/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27665,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27671,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138191,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1669aa/report-thumb.jpg"},{"id":27670,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1669aa/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696a4d","contributors":{"authors":[{"text":"Leggat, E. R.","contributorId":28222,"corporation":false,"usgs":true,"family":"Leggat","given":"E. R.","affiliations":[],"preferred":false,"id":144671,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lowry, M.E.","contributorId":55807,"corporation":false,"usgs":true,"family":"Lowry","given":"M.E.","email":"","affiliations":[],"preferred":false,"id":144672,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hood, J. W.","contributorId":87908,"corporation":false,"usgs":true,"family":"Hood","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":144673,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2065,"text":"wsp1578 - 1964 - Geology and ground-water resources of the Bristol-Plainville-Southington area, Connecticut","interactions":[],"lastModifiedDate":"2023-01-11T19:59:47.775386","indexId":"wsp1578","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":"1578","title":"Geology and ground-water resources of the Bristol-Plainville-Southington area, Connecticut","docAbstract":"The Bristol-Plainville-Southington area straddles the boundary between the New England Upland and the Connecticut Valley Lowland sections of the New England physiographic province. The western parts of Bristol are Southington lie in the New England Upland section, an area of rugged topography underlain by metamorphic rocks of Palezoic age. The eastern part of the area, to the east of a prominent scarp marking the limit of the metamorphic rocks, is in the Connecticut Valley Lowland and is underlain by sedimentary rocks and interbedded basaltic lava flows of Triassic age. The lowland is characterized for the most part by broad valleys and low intervening linear hills, but in the eastern parts of Plainville and Southington, basaltic rocks form a rugged highland. The bedrock is largely mantled by glacial deposits of Wisconsin age. On hills the glacial deposits are mainly ground moraine, and in valleys mainly stratified. The metamorphic rocks comprise the Hartland Formation, Bristol Granite Gneiss of Gregory (1906), and Prospect Gneiss. These formations contain water in fractures, principally joints occurring in regular sets. The rocks generally yield supplies of 5 to 15 gpm (gallons per minute) to drilled wells averaging about 140 feet in depth. \r\n\r\nThe rocks of Triassic age in the area are the New Haven Arkose, Talcott Basalt, Shuttle Meadow Formation, Holyoke Basalt, and East Berlin Formation. The formations contain water principally in joints and other fractures and, to a lesser extent, in bedding-plane openings and pore spaces. Drilled wells penetrating these rocks generally range from 100 to 200 feet in depth and yield an average of nearly 20 gpm. The maximum yield obtained from a well in these rocks is 180 gpm. \r\n\r\nThe ground moraine of Pleistocene age is composed principally of till. The deposit averages about 24 feet in thickness, and wells penetrating it average about 16 feet in depth. The ground moraine yields small supplier of water suitable for household use when tapped by shallow large-diameter wells. The stratified glacial deposits, which are as much as 300 feet thick, comprise ice-contact and proglacial deposits and deposits of generally obscure origin termed 'undifferentiated stratified deposits.' The ice-contact and undifferentiated stratified deposits, some of which underlie proglacial deposits, are coarse grained and contain gravel beds from which supplies of as much as 1,400 gpm can be obtained. The proglacial deposits are, on the whole, finer grained than the other stratified deposits, but in places they allow development of wells producing as much as 500 gpm. However, the stratified glacial deposits throughout much of the Bristol-Plainville-Southington area are fine grained and provide only small supplies.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1578","usgsCitation":"La Sala, A., 1964, Geology and ground-water resources of the Bristol-Plainville-Southington area, Connecticut: U.S. Geological Survey Water Supply Paper 1578, Report: iv, 70 p.; 3 Plates: 31.00 × 37.03 inches or smaller, https://doi.org/10.3133/wsp1578.","productDescription":"Report: iv, 70 p.; 3 Plates: 31.00 × 37.03 inches or smaller","costCenters":[],"links":[{"id":27619,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1578/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27618,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1578/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27617,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1578/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27616,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1578/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138433,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1578/report-thumb.jpg"},{"id":397416,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24764.htm"}],"scale":"24000","country":"United States","state":"Connecticut","city":"Bristol, Plainville, Southington","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72.998,\n 41.546\n ],\n [\n -72.817,\n 41.546\n ],\n [\n -72.817,\n 41.723\n ],\n [\n -72.998,\n 41.723\n ],\n [\n -72.998,\n 41.546\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cee4b07f02db5458ec","contributors":{"authors":[{"text":"La Sala, A. M.","contributorId":103659,"corporation":false,"usgs":true,"family":"La Sala","given":"A. M.","affiliations":[],"preferred":false,"id":144625,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5978,"text":"pp431 - 1964 - Geology and mineral deposits of the Osgood Mountains quadrangle, Humboldt County, Nevada","interactions":[],"lastModifiedDate":"2013-06-26T12:51:45","indexId":"pp431","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":"431","title":"Geology and mineral deposits of the Osgood Mountains quadrangle, Humboldt County, Nevada","docAbstract":"The Osgood Mountains quadrangle is in north-central Nevada northeast of Winnemucca, the principal town in the region. The quadrangle includes two north-northeast-trending mountain ranges, the Osgood Mountains on the east and the Hot Springs Range on the west, which are separated by a narrow valley and\nare bounded on the east and west by broad alluviated basins. Large deposits of tungsten and gold have been mined in the northeastern part of the Osgood Mountains; small deposits of quicksilver, lead, zinc, and gold are known in the Hot Springs Range, and some prospecting has been done on barite deposits\nin the Osgood Mountains. Some quartzite beds are potential sources of silica.","language":"ENGLISH","publisher":"United States Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp431","usgsCitation":"Hotz, P.E., and Willden, C.R., 1964, Geology and mineral deposits of the Osgood Mountains quadrangle, Humboldt County, Nevada: U.S. Geological Survey Professional Paper 431, vi, 128 p., https://doi.org/10.3133/pp431.","productDescription":"vi, 128 p.","costCenters":[],"links":[{"id":104457,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4425.htm","linkFileType":{"id":5,"text":"html"},"description":"4425"},{"id":139770,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0431/report-thumb.jpg"},{"id":268952,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0431/report.pdf"}],"country":"United States","state":"Nevada","county":"Humboldt County","otherGeospatial":"Osgood Mountains Quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -12,8.333333333333334E-4 ], [ -12,0.0011111111111111111 ], [ -11.066666666666666,0.0011111111111111111 ], [ -11.066666666666666,8.333333333333334E-4 ], [ -12,8.333333333333334E-4 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b46ca","contributors":{"authors":[{"text":"Hotz, Preston Enslow","contributorId":15191,"corporation":false,"usgs":true,"family":"Hotz","given":"Preston","email":"","middleInitial":"Enslow","affiliations":[],"preferred":false,"id":151901,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Willden, Charles Ronald","contributorId":84388,"corporation":false,"usgs":true,"family":"Willden","given":"Charles","email":"","middleInitial":"Ronald","affiliations":[],"preferred":false,"id":151902,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2905,"text":"wsp1584 - 1964 - Geology and ground-water resources of Uvalde County, Texas","interactions":[],"lastModifiedDate":"2016-08-22T10:54:28","indexId":"wsp1584","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":"1584","title":"Geology and ground-water resources of Uvalde County, Texas","docAbstract":"The principal aquifer in Uvalde County is the Edwards and associated limestones of Cretaceous age. The aquifer underlies an extensive area in south-central Texas extending along the Balcones fault zone from Kinney County eastward to San Antonio, and thence northeastward to Hays County. The hydrologic unit making up the Edwards and associated limestones consists of the Comanche Peak limestone, the Edwards limestone, the Kiamichi formation, and the Georgetown limestone. Other less important aquifers in Uvalde County include the Glen Rose limestone, the Buda limestone, the Austin chalk, and the Leona formation.
\n\n
Uvalde County occupies parts of two physiographic provinces, the Edwards Plateau on the north and the Coastal Plain on the south; the two provinces are separated by the Balcones fault zone. In the Edwards Plateau the formations of the Edwards and associated limestones crop out on the plateau surface; in the Coastal Plain where the formations have been down-faulted, they underlie younger rocks. In both provinces the formations dip gently toward the south and southeast; the dips are greatest in the Coastal Plain. Igneous intrusions have penetrated the formations in many places in the Coastal Plain, and locally have formed barriers to ground-water movement.
\n\n
The aquifers in Uvalde County are recharged by precipitation within the county and in the drainage areas of streams entering the county from the north and west. In the Edwards Plateau, the Edwards and associated limestones are recharged by precipitation that falls on the outcrop. The aquifer is drained by springs at the contact with the underlying Glen Rose limestone where streams have cut through the Edwards at the edge of the plateau. These springs maintain the base flow of the streams that drain the plateau. Most of the base flow and much of flood flow of the streams is lost to the Edwards and associated limestones where they crop out in streambeds in the Balcones fault zone. This stream loss to the aquifer constitutes the greatest part of the recharge in the county, although some of the recharge from the West Nueces River enters the county as underflow from Kinney County. The normal annual recharge to the Edwards in Uvalde County is estimated to be about 200,000 acre-feet.
\n\n
Discharge from the Edwards and associated limestones in Uvalde County can be divided into two .major segments: discharge by underflow from the county to the east and south and discharge to the surface through wells and springs. Discharge by underflow during the period 1934-47, when changes in storage were small, is estimated to have been about 190,000 acre-feet per year. During the drought years 1947-56 the underflow was somewhat less. The discharge to the surface during 1934-47 averaged about 17,000 acre-feet per year. During the 1947-56 drought the rate of discharge to the surface increased principally because of increased use of water for irrigation, reaching a maximum of 58,000 acre-feet in 1956.
\n\n
The chemical quality. of the ground water in Uvalde County ranges between wide limits. Except in the extreme southern part of the county where the water is saline, the water in the Edwards and associated limestones is of good chemical quality except that it is hard. The water in the Glen Rose limestone is saline in many places; the principal objectionable constituents are high concentrations of calcium and magnesium sulfate. The water in the Leona formation is generally of good chemical quality. The water from the other formations varies widely in quality from place to place and no generalizations can be made.
\n\n
Ground-water withdrawals from the Edwards and associated limestones in Uvalde County probably could be maintained indefinitely at a rate of about 200,000 acre-feet per year, provided that withdrawals north and west of the county were not increased. However, continued withdrawals at this rate-would cause wells in structurally high areas to go dry, and underflow into Medina County would cease. Furthermore, saline water might invade the fresh-water part of the aquifer from the south, and perennial spring flow in the Leona River valley would cease.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1584","collaboration":"Prepared in cooperation with the Texas Board of Water Engineers and the City of San Antonio","usgsCitation":"Welder, F., and Reeves, R., 1964, Geology and ground-water resources of Uvalde County, Texas: U.S. Geological Survey Water Supply Paper 1584, Report: v, 49 p.; 12 Plates: 28 x 28 inches or smaller, https://doi.org/10.3133/wsp1584.","productDescription":"Report: v, 49 p.; 12 Plates: 28 x 28 inches or smaller","numberOfPages":"57","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":29585,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":110058,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25579.htm","linkFileType":{"id":5,"text":"html"},"description":"25579"},{"id":29586,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29587,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29588,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29589,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29590,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29591,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29592,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29593,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29594,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29595,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29596,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1584/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138405,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1584/report-thumb.jpg"},{"id":277928,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1584/report.pdf"}],"scale":"125000","country":"United States","state":"Texas","county":"Uvalde County","city":"San Antonio","otherGeospatial":"Coastal Plain;Edwards Plateau;West Nueces River","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -101.0,28.0 ], [ -101.0,31.0 ], [ -97.0,31.0 ], [ -97.0,28.0 ], [ -101.0,28.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685977","contributors":{"authors":[{"text":"Welder, F.A.","contributorId":104878,"corporation":false,"usgs":true,"family":"Welder","given":"F.A.","email":"","affiliations":[],"preferred":false,"id":145987,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reeves, R.D.","contributorId":95043,"corporation":false,"usgs":true,"family":"Reeves","given":"R.D.","email":"","affiliations":[],"preferred":false,"id":145986,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1219,"text":"wsp1693 - 1964 - A summary of the occurrence and development of ground water in the southern High Plains of Texas","interactions":[],"lastModifiedDate":"2022-12-30T22:35:11.105123","indexId":"wsp1693","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1964","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1693","title":"A summary of the occurrence and development of ground water in the southern High Plains of Texas","docAbstract":"The Southern High Plains of Texas occupies an area of about 22,000 square miles in northwest Texas, extending from the Canadian River southward. about 250 miles and from the New Mexico line eastward an average distance of about 120 miles.
The economy of the area is dependent largely upon irrigated agriculture, and in 1958 about 44,000 irrigation wells were in operation. The economy of the area is also dependent upon the oil industry either in the form of oil and gas production or in the form of industries based on the production of petroleum.
The Southern High Plains of Texas is characterized by a nearly flat land surface sloping gently toward the southeast at an average of 8 to 10 feet per mile. Shallow undrained depressions or playas are characteristic of the plains surface, and during periods of heavy rainfall, runoff collects in the depressions to form temporary ponds or lakes. Stream drainage on the plains surface is poorly developed; water discharges over the eastern escarpment off the plains only during periods of excessive rainfall.
The climate of the area is semiarid; the average annual precipitation is about 20 inches. About 70 percent of the precipitation falls during the growing season from April to September.
Rocks of Permian age underlie the entire area and consist chiefly of red sandstone and shale containing numerous beds of gypsum and dolomite. The Permian rocks are not a source of water in the Southern High Plains, and any water in these rocks would probably be saline.
The Triassic rocks underlying the Southern High Plains consist of three formations of the Dockum group: the Tecovas formation, the Santa Rosa sandstone. and the Chinle formation equivalent. The Tecovas and Chinle formation equivalent both consist chiefly of shale and sandy shale; however, the Santa Rosa sandstone consists mainly of medium to coarse conglomeratic sandstone containing some shale. The formations of the Dockum group are capable of yielding small to moderate quantities of water in many parts of the Southern High Plains; however, in practically all places the water is rather saline and probably unsuitable for most uses.
The Cretaceous formations in the Southern High Plains consist of several formations of the Trinity, Fredericksburg, and Washita groups. The rocks underlie a large part of the southern part of the Southern High Plains; they consist of sandstone, shale, and limestone, the sandstone and limestone being the principal water-bearing units. In a few places where the Cretaceous rocks appear to be in hydraulic connection with the overlying Ogallala formation, moderate quantities of water are obtained, particularly from the limestones. Locally the Cretaceous rocks may be important aquifers where other water is not available, but they generally do not constitute a large source of water for irrigation or municipal use.
The Ogallala formation of Pliocene age is the principal aquifer in the Southern High Plains of Texas; it supplies practically all the water used for all purposes. The formation is continuous throughout most of the Texas part of the Southern High Plains and extends into New Mexico. The .formation consists chiefly of sediments deposited by streams that had their headwaters in the mountainous regions to the west and northwest. The Ogallala formation rests unconformably upon an erosional surface of the underlying Triassic and Cretaceous rocks. The Ogallala consists of beds and lenses of clay, silt, sand, and gravel; caliche occurs as a secondary deposit ,in many places in the formation. In general the Ogallala is thicker in the northern part of the area; the thickness ranges from 400 to 500 feet in central Parmer, west-central Castro, and southwestern Floyd Counties to a knife edge where the formation wedges out against outcrops of the older rocks.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1693","usgsCitation":"Cronin, J., and Myers, B.N., 1964, A summary of the occurrence and development of ground water in the southern High Plains of Texas: U.S. Geological Survey Water Supply Paper 1693, Report: v, 88 p.; 7 Plates: 13.00 x 23.50 inches or smaller, https://doi.org/10.3133/wsp1693.","productDescription":"Report: v, 88 p.; 7 Plates: 13.00 x 23.50 inches or smaller","costCenters":[],"links":[{"id":26128,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26130,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26129,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26131,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":411263,"rank":10,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24899.htm","linkFileType":{"id":5,"text":"html"}},{"id":26127,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26132,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1693/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137997,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1693/report-thumb.jpg"},{"id":26126,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26125,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1693/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -99.9,\n 36.85\n ],\n [\n -104.481,\n 36.85\n ],\n [\n -104.481,\n 31.61\n ],\n [\n -99.9,\n 31.61\n ],\n [\n -99.9,\n 36.85\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a5f28","contributors":{"authors":[{"text":"Cronin, J.G.","contributorId":47769,"corporation":false,"usgs":true,"family":"Cronin","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":143387,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Myers, B. N.","contributorId":67490,"corporation":false,"usgs":true,"family":"Myers","given":"B.","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":143388,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":6204,"text":"pp469 - 1964 - Cambrian rocks of the Pioche mining district, Nevada: With a section on Pioche shale faunules","interactions":[],"lastModifiedDate":"2022-01-11T19:22:58.368205","indexId":"pp469","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":"469","title":"Cambrian rocks of the Pioche mining district, Nevada: With a section on Pioche shale faunules","docAbstract":"The Pioche mining district in the Ely Range, southeastern Nevada, is one of several districts in the Great Basin where Cambrian rocks are hosts of important ore deposits. Cambrian strata underlying the Ely Range are intruded by porphyritic granite and other dikes. Tertiary volcanic rocks and Pliocene fresh-water clastic deposits of the Panaca Formation occupy adjacent valleys and extend over the Cambrian strata on the south and east.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/pp469","usgsCitation":"Merriam, C.W., and Palmer, A.R., 1964, Cambrian rocks of the Pioche mining district, Nevada: With a section on Pioche shale faunules: U.S. Geological Survey Professional Paper 469, Report: iv, 59 p.; 1 Plate: 19.43 × 17.94 inches, https://doi.org/10.3133/pp469.","productDescription":"Report: iv, 59 p.; 1 Plate: 19.43 × 17.94 inches","costCenters":[],"links":[{"id":394196,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4473.htm"},{"id":274603,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0469/plate-1.pdf"},{"id":268957,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0469/report.pdf"},{"id":140077,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0469/report-thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Pioche mining district","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.75,\n 37.75\n ],\n [\n -114.3333,\n 37.75\n ],\n [\n -114.3333,\n 38.1203\n ],\n [\n -114.75,\n 38.1203\n ],\n [\n -114.75,\n 37.75\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a04e4b07f02db5f855e","contributors":{"authors":[{"text":"Merriam, Charles Warren","contributorId":14399,"corporation":false,"usgs":true,"family":"Merriam","given":"Charles","email":"","middleInitial":"Warren","affiliations":[],"preferred":false,"id":152295,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Palmer, Allison R.","contributorId":24343,"corporation":false,"usgs":true,"family":"Palmer","given":"Allison","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":152296,"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":20670,"text":"ofr64135 - 1964 - Preliminary report on the geologic and geophysical investigations of the Loveland Basin landslide, Clear Creek County, Colorado","interactions":[],"lastModifiedDate":"2025-06-12T16:13:35.631834","indexId":"ofr64135","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":"64-135","title":"Preliminary report on the geologic and geophysical investigations of the Loveland Basin landslide, Clear Creek County, Colorado","docAbstract":"Geologic and geophysical investigations of the Loveland Basin landslide, which formed at the cut for the east portal of the Straight Creek tunnel, were made by the U.S. Geological Survey in cooperation with the U.S. Bureau of Public Road and the Colorado Department of Highways. The investigations indicate that the slide has a probable minimum volume of 500,000 cubic yards weighing 1,000,000 tons and probable maximum volume of 770,000 cubic yards weighing 1,600,000 tons.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr64135","usgsCitation":"Robinson, C., Carroll, R.D., and Lee, F.T., 1964, Preliminary report on the geologic and geophysical investigations of the Loveland Basin landslide, Clear Creek County, Colorado: U.S. Geological Survey Open-File Report 64-135, Report: 5 p.; 6 Figures: 27.62 x 22.74 inches or smaller, https://doi.org/10.3133/ofr64135.","productDescription":"Report: 5 p.; 6 Figures: 27.62 x 22.74 inches or smaller","costCenters":[],"links":[{"id":153128,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1964/0135/report-thumb.jpg"},{"id":490564,"rank":8,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1964/0135/figure-6.pdf","text":"Figure 6","linkFileType":{"id":1,"text":"pdf"}},{"id":490563,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1964/0135/figure-5.pdf","text":"Figure 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66c94f","contributors":{"authors":[{"text":"Robinson, Charles Sherwood 0000-0002-7623-2380","orcid":"https://orcid.org/0000-0002-7623-2380","contributorId":71163,"corporation":false,"usgs":true,"family":"Robinson","given":"Charles Sherwood","affiliations":[],"preferred":false,"id":183038,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carroll, R. D.","contributorId":53373,"corporation":false,"usgs":true,"family":"Carroll","given":"R.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":940195,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lee, Fitzhugh T.","contributorId":82272,"corporation":false,"usgs":true,"family":"Lee","given":"Fitzhugh","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":183039,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":6304,"text":"pp449 - 1964 - Geology of the central and northern parts of the Western Cascade Range in Oregon","interactions":[{"subject":{"id":15363,"text":"ofr60110 - 1960 - Geologic reconnaissance of the Western Cascades in Oregon north of latitude 43 degrees","indexId":"ofr60110","publicationYear":"1960","noYear":false,"title":"Geologic reconnaissance of the Western Cascades in Oregon north of latitude 43 degrees"},"predicate":"SUPERSEDED_BY","object":{"id":6304,"text":"pp449 - 1964 - Geology of the central and northern parts of the Western Cascade Range in Oregon","indexId":"pp449","publicationYear":"1964","noYear":false,"title":"Geology of the central and northern parts of the Western Cascade Range in Oregon"},"id":1}],"lastModifiedDate":"2017-06-10T11:35:34","indexId":"pp449","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":"449","title":"Geology of the central and northern parts of the Western Cascade Range in Oregon","docAbstract":"This report pt·esents a description of the stratigraphy, structure, and petrology of the volcanic rocks of the central and northern parts of the Western Cascade Range of Oregon. The study is a part of a long-range cooperative program between the U.S. Geological Survey and the Oregon State Department of Geology and Mineral Industries to prepare a geologic map of Oregon. The map area, about 7,500 square miles, lies in the densely forested western slope of the Cascade Range. It is bounded approximately by lat 43° N. and lat 45°30' N. on the south and north, the crest of the range on the east, and long 123° W. and the edge of the Willamette Valley on the west. The geology, which was mapped by reconnaissance methods, is chiefly based on examination of rock exposures along roads. The Cascade Range in Oregon comprises two physiographic divisions: the Western Cascade Range, which includes a wide, deeply dissected belt of volcanic formations making up the western slope of the range, and the High Cascade Range, which includes chiefly younger cones and lava flows forming the nearly undissected crest of the range. The volcanic rocks of the Western Cascade Range are deformed and partially altered flows and pyroclastic rocks that range in age from late Eocene t·o lute Miocene, as determined chiefly from fossil plants from more than 50 localities. These volcanic rocks overlie or interfinger westward with marine sedimentary rocks, and in the southwestern part of the map area they overlie pre-Tertiary plutonic and metamorphic rocks of the Klamath Mountains.","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp449","usgsCitation":"Peck, D.L., Griggs, A., Schlicker, H.G., Wells, F., and Dole, H.M., 1964, Geology of the central and northern parts of the Western Cascade Range in Oregon: U.S. Geological Survey Professional Paper 449, Report: iv, 56 p.; 1 Plate, https://doi.org/10.3133/pp449.","productDescription":"Report: iv, 56 p.; 1 Plate","numberOfPages":"62","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":112791,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0449/report.pdf","size":"11963","linkFileType":{"id":1,"text":"pdf"}},{"id":139781,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0449/report-thumb.jpg"},{"id":263467,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0449/plate-1.jpg"}],"country":"United States","state":"Oregon","otherGeospatial":"Cascades","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -123.0,43.0 ], [ -123.0,45.5 ], [ -121.0,45.5 ], [ -121.0,43.0 ], [ -123.0,43.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c8b4","contributors":{"authors":[{"text":"Peck, Dallas L.","contributorId":60187,"corporation":false,"usgs":true,"family":"Peck","given":"Dallas","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":152476,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Griggs, Allan B.","contributorId":21929,"corporation":false,"usgs":true,"family":"Griggs","given":"Allan B.","affiliations":[],"preferred":false,"id":152474,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Schlicker, Herbert G.","contributorId":7151,"corporation":false,"usgs":true,"family":"Schlicker","given":"Herbert","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":152473,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wells, Francis G.","contributorId":40582,"corporation":false,"usgs":true,"family":"Wells","given":"Francis G.","affiliations":[],"preferred":false,"id":152475,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Dole, Hollis M.","contributorId":68185,"corporation":false,"usgs":true,"family":"Dole","given":"Hollis","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":152477,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":3004,"text":"wsp1786 - 1964 - Inventory of published and unpublished chemical analyses of surface waters in the continental United States and Puerto Rico, 1961","interactions":[],"lastModifiedDate":"2017-09-06T17:54:41","indexId":"wsp1786","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":"1786","title":"Inventory of published and unpublished chemical analyses of surface waters in the continental United States and Puerto Rico, 1961","docAbstract":"This inventory contains a list of published and unpublished chemical analyses obtained through September 30, 1961, by agencies associated with the Subcommittee on Hydrology. Bulletin 6 of Subcommittee on Hydrology includes references to all surface-water analyses for states east of the Mississippi River known to exist in the files of Federal agencies through September 30, 1951. Records of analyses of surface waters for states west of the Mississippi River are included in Bulletins 2 and 9 of the Subcommittee. Bulletin 2 includes the period of record prior to October 1, 1947, and Bulletin 9 includes the period from October 1, 1947, to September 30, 1955. Therefore, the earliest date for which references to data are included in this volume varies from October 1951 for states east of the Mississippi River (including Minnesota) to October 1, 1955, for states west of the Mississippi River. Analyses of water from Alaska and Puerto Rico were not reported in earlier inventories. An attempt was made to include available analyses obtained in Alaska since October 1951, but additional chemical determinations of water in Alaska that are not inventoried in this report were undoubtedly made in years prior to 1951. Requests concerning specific records not reported herein should be directed to offices having responsibility in the area.
This publication is patterned after preceding bulletins as far as practicable. The contents include a list of sampling stations and locations, drainage area above each station, period of record, number and frequency of samples collected, number of analytical values reported in each group arranged according to general types or purposes, and a list of references to the sources of basic data.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1786","collaboration":"Prepared in cooperation with the Subcommittee on Hydrology, Inter-Agency Committee on Water Resources","usgsCitation":"Woodard, T.H., and Heidel, S.G., 1964, Inventory of published and unpublished chemical analyses of surface waters in the continental United States and Puerto Rico, 1961: U.S. Geological Survey Water Supply Paper 1786, v, 490 p., https://doi.org/10.3133/wsp1786.","productDescription":"v, 490 p.","numberOfPages":"496","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":29798,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1786/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139406,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1786/report-thumb.jpg"}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66ce7f","contributors":{"authors":[{"text":"Woodard, Thomas H.","contributorId":106102,"corporation":false,"usgs":true,"family":"Woodard","given":"Thomas","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":146135,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heidel, Sumner Griggs","contributorId":97082,"corporation":false,"usgs":true,"family":"Heidel","given":"Sumner","email":"","middleInitial":"Griggs","affiliations":[],"preferred":false,"id":146134,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}