The U.S. Soil Conservation Service is actively engaged in the installation of flood and soil erosion reducing measures in Texas under the authority of \"The Flood Control Act of 1936 and 1944\" and \"Watershed Protection and Flood Prevention Act\" (Public Law 566), as amended. The Soil Conservation Service has found a total of approximately 3,500 floodwater-retarding structures to be physically and economically feasible in Texas. As of September 30, 1969, 1,355 of these structures had been built.
This watershed-development program will have varying but important effects on the natural surface- and ground-water resources of river basins, especially where a large number of the floodwater-retarding structures are built. Basic hydrologic data under natural and developed conditions are needed to appraise the effects of the structures on the yield and mode of occurrence of runoff.
Hydrologic investigations of these small watersheds were begun by the U.S. Geological Survey in 1951 and are now being made in 12 areas (fig. 1). These studies are being made in cooperation with the Texas Water Development Board, the Soil Conservation Service, the San Antonio River Authority, the city of Dallas, and the Tarrant County Water Control and Improvement District No. 1. The 12 study areas were chosen to sample watersheds having different rainfall, topography, geology, and soils. In five of the study areas (North, Little Elm, Mukewater, North Elm-Little Pond, and Pin Oak Creeks), streamflow and rainfall records were collected prior to construction of the floodwater-retarding structures, thus affording the opportunity for analyses of the conditions \"before and after\" development. Structures have now been built in three of these study areas. A summary of the development of the floodwater-retarding structures on each study area as of September 30, 1969, is shown in table 1.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr71144","collaboration":"Prepared in cooperation with the Texas Water Development Board","usgsCitation":"Hampton, B., and Myers, D., 1971, Annual compilation and analysis of hydrologic data for Pin Oak Creek, Trinity River basin, Texas, 1969: U.S. Geological Survey Open-File Report 71-144, iii, 28 p., https://doi.org/10.3133/ofr71144.","productDescription":"iii, 28 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":389294,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0144/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":162569,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0144/report-thumb.jpg"}],"country":"United States","state":"Texas","otherGeospatial":"Pin Oak Creek, Trinity River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.90765380859375,\n 31.344254455668054\n ],\n [\n -96.12487792968749,\n 31.344254455668054\n ],\n [\n -96.12487792968749,\n 31.891550612684366\n ],\n [\n -96.90765380859375,\n 31.891550612684366\n ],\n [\n -96.90765380859375,\n 31.344254455668054\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67bbb4","contributors":{"authors":[{"text":"Hampton, B.B.","contributorId":43362,"corporation":false,"usgs":true,"family":"Hampton","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":236547,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Myers, D.R.","contributorId":104534,"corporation":false,"usgs":true,"family":"Myers","given":"D.R.","email":"","affiliations":[],"preferred":false,"id":236548,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2606,"text":"wsp1896 - 1971 - Ground-water hydrology of the San Pitch River drainage basin, Sanpete County, Utah","interactions":[],"lastModifiedDate":"2017-09-04T12:52:56","indexId":"wsp1896","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"1896","title":"Ground-water hydrology of the San Pitch River drainage basin, Sanpete County, Utah","docAbstract":"The San Pitch River drainage basin in central Utah comprises an area of about 850 square miles; however, the investigation was concerned primarily with the Sanpete and Arapien Valleys, which comprise about 250 square miles and contain the principal ground-water reservoirs in the basin. Sanpete Valley is about 40 miles long and has a maximum width of 13 miles, and Arapien Valley is about 8 miles long and 1 mile wide. The valleys are bordered by mountains and plateaus that range in altitude from 5,200 to 11,000 feet above mean sea level.
The average annual precipitation on the valleys is about 12 inches, but precipitation on the surrounding mountains reaches a maximum of about 40 inches per year. Most of the precipitation on the mountains falls as snow, and runoff from snowmelt during the spring and summer is conveyed to the valleys by numerous tributaries of the San Pitch River. Seepage from the tributary channels and underflow beneath the channels are the major sources of recharge to the ground-water reservoir in the valleys.
Unconsolidated valley fill constitutes the main ground-water reservoir in Sanpete and Arapien Valleys. The fill, which consists mostly of coalescing alluvial fans and flood deposits of the San Pitch River, ranges in particle size from clay to boulders. Where they are well sorted, these deposits yield large quantities of water to wells.
Numerous springs discharge from consolidated rocks in the mountains adjacent to the valleys and along the west margin of Sanpete Valley, which is marked by the Sevier fault. The Green River Formation of Tertiary age and several other consolidated formations yield small to large quantities of water to wells in many parts of Sanpete Valley. Most water in the bedrock underlying the valley is under artesian pressure, and some of this water discharges upward into the overlying valley fill.
The water in the valley fill in Sanpete Valley moves toward the center of the valley and thence downstream. The depth to water along parts of the sides of the valley is more than 100 feet, but in much of the central part of the valley, the water level is at or above the land surface. The valley fill pinches out in the southern part of the valley, and most of the ground water moves to the surface, where it discharges into the San Pitch River or is consumed by evapotranspiration.
Ground water is discharged principally by wells, springs, and evapotranspiration. The discharge from wells varies considerably from year to year because most of the water is used for irrigation, and the wells are used only as necessary to supplement the available surface-water supply. Thus, in 1965, a year of above-normal precipitation, the discharge from wells was 12,000 acre-feet, whereas in 1966, a year of below-normal precipitation, the wells discharged 21,000 acre-feet. The discharge from springs during 1966 was estimated to be 36,000 acre-feet, and an additional 113,000 acre-feet of water was discharged by phreatophytes.
Water levels in the valleys, for the most part, fluctuate in direct response to variations in precipitation, and the discharge from wells has had little long-term effect on water levels. Approximately 3 million acre-feet of water available to wells is stored in the upper 200 feet of saturated valley fill.
The ground water in most parts of the valleys is fresh and suitable for public supply and irrigation. The Green River and Crazy Hollow Formations may, in some places, yield slightly or moderately saline water.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1896","collaboration":"Prepared in cooperation with the Utah Department of Natural Resources","usgsCitation":"Robinson, G.B., 1971, Ground-water hydrology of the San Pitch River drainage basin, Sanpete County, Utah: U.S. Geological Survey Water Supply Paper 1896, Report: v, 80 p.; 4 Plates: 53.00 in. x 33.50 in. or smaller, https://doi.org/10.3133/wsp1896.","productDescription":"Report: v, 80 p.; 4 Plates: 53.00 in. x 33.50 in. or smaller","numberOfPages":"88","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":28889,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1896/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Generalized geologic map and sections showing location of selected hydrologic data series, San Pitch River drainage basin, Sanpete County, Utah"},{"id":28890,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1896/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Hydrlogic maps of the San Pitch River drainage basin, Sanpete County, Utah"},{"id":28891,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1896/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Hydrographs of selected wells in the San Pitch River drainage basin, Sanpete County, Utah, for all or part of the period 1937-67, and graph showing cumulative departure from the 1931-60 normal anual precipitation at Manti"},{"id":28892,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1896/plate-4.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing generali chemical quality of the ground and surface waters, as indicated by specific conductance, in the San Pitch River drainage basin, Sanpete County, Utah"},{"id":28893,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1896/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138705,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1896/report-thumb.jpg"},{"id":110032,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25114.htm","linkFileType":{"id":5,"text":"html"},"description":"25114"}],"country":"United States","state":"Utah","county":"Sanpete County","otherGeospatial":"San Pitch River drainage basin","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65e66d","contributors":{"authors":[{"text":"Robinson, Gerald B. Jr.","contributorId":91837,"corporation":false,"usgs":true,"family":"Robinson","given":"Gerald","suffix":"Jr.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":145484,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2852,"text":"wsp1899E - 1971 - Ground water for irrigation in the Brooten-Belgrade area, west-central Minnesota","interactions":[],"lastModifiedDate":"2018-04-02T12:00:47","indexId":"wsp1899E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"1899","chapter":"E","title":"Ground water for irrigation in the Brooten-Belgrade area, west-central Minnesota","docAbstract":"Water for irrigation is needed to improve crop yields from sandy soils in the Brooten-Belgrade area. Ground-water supplies of sufficient quantity and suitable quality for irrigation are available in much of the area.
\nQuaternary glacial drift, as much as 300 feet thick, is underlain by Precambrian crystalline rocks and possibly by Cretaceous sedimentary rocks. Sand and gravel aquifers are buried at various depths in the drift and can be located by test drilling. One buried aquifer, possibly capable of high yields, is within 250 feet of the land surface in the vicinity of Belgrade.
\nGlacial outwash comprises the upper part of the drift in most of the project area and is locally more than 100 feet thick. The outwash is made up of crossbedded sand and gravel that is interbedded in places with silt and clay deposits and has a saturated thickness of as much as 65 feet. Locally, the transmissivity of the surficial aquifer is as much as 60,000 gallons per day per foot, but elsewhere is generally less than 30,000 gallons per day per foot. The aquifer should yield more than 300 gallons per minute and locally more than 1,000 gallons per minute to individual wells in much of the northern and southwestern parts of the area.
\nRecharge to the surficial aquifer is almost entirely from precipitation. Significant ground-water losses occur as base flow and underflow, and through evaporation and transpiration.
\nWater in the buried and surficial aquifers is of the calcium magnesium bicarbonate type and is of suitable quality for irrigation.
\nAn analog model, simulating yearly 30-day pumping periods and hypothetical volumes and distributions of withdrawals, showed the effects on the surficial aquifer of withdrawals of about 20,000 acre-feet per pumping season for 20 years. Predicted water-level declines caused by withdrawals of 20,000 acre-feet per pumping season were generally less than 5 feet in the surficial aquifer and years Predicted water-level declines caused by withdrawals of 20,000 acre-feet pumping season caused predicted water-table declines of more than 10 feet in large parts of the area and caused lake-level declines of as much as 8 feet. The model indicated that water removed from aquifer and lake storage accounted for less than 50 percent of all withdrawals; the remainder was accounted for by water recovered from stream base flow and by water diverted from evaporation and transpiration.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1899E","collaboration":"Prepared in cooperation with the West-Central Minnesota Resource Conservation and Development Committee and the Minnesota Department of Conservation, Division of Waters, Soils, and Minerals","usgsCitation":"Van Voast, W.A., 1971, Ground water for irrigation in the Brooten-Belgrade area, west-central Minnesota: U.S. Geological Survey Water Supply Paper 1899, Document: iv, 24 p.; 2 Plates: 35 x 40 inches and 37 x 39 inches, https://doi.org/10.3133/wsp1899E.","productDescription":"Document: iv, 24 p.; 2 Plates: 35 x 40 inches and 37 x 39 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":110036,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25120.htm","linkFileType":{"id":5,"text":"html"},"description":"25120"},{"id":29441,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1899e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29442,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1899e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29443,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1899e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139069,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1899e/report-thumb.jpg"}],"country":"United States","state":"Minnesota","otherGeospatial":"Brooten-Belgrade area","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -95.22468566894531, 45.44038088829218 ], [ 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,{"id":925,"text":"wsp1999C - 1971 - Water resources of the upper White River basin, east-central Indiana","interactions":[],"lastModifiedDate":"2022-11-07T16:50:28.66113","indexId":"wsp1999C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"1999","chapter":"C","title":"Water resources of the upper White River basin, east-central Indiana","docAbstract":"Ground-water discharge to the streams sustains year-round streamflow in the upper White River basin. This discharge, referred to as ground-water runoff or base runoff, is considered to be an index to the amount of g ound water available for development. A comparison of the variations of groundwater runoff and aquifer distribution in the basin shows that the areas of best development potential are areas where thick sand and gravel aquifers are adjacent to the streams. The average ground-water runoff for these areas is between 400,000 and 500,000 gallons per day per square mile.
\nThe most permeable aquifers in the basin are the sand and gravel deposits of Quaternary age. These aquifers occur mainly as relatively thick elongate bodies along bedrock valleys and as relatively thin sheetlike deposits at or near land surface. The representative hydraulic conductivity of these aquifers ranges from 1,500 to 2,500 gallons per day per square foot. The limestone and dolomite formations of the bedrock are a source of moderate quar tities of water.
\nThe long-term average streamflow in the basin is approximately 0.9 cubic feet per second per square mile. The yearly average discharge varies from about one-fourth to twice the long-term average. The 7-day 10-year low flow ranges from about 0.01 to 0.3 cubic feet per second per square mile; the main-stem flow ranges from 0.10 to 0.13 cubic feet per second per square mile.
\nThe water in the aquifers is predominately a very hard calcium bicarbonate type; it is generally high in iron and contains a moderate amount of dissolved solids. Fresh water (1,000 milligrams per liter dissolved solids or less) is present to depths of approximately 400 feet below land surface. In the tributaries and in the headwaters region of the White River, the composition of surface water is very similar to that of ground water. The quality cf the water in the White River deteriorates in the downstream direction owing to the cumulative effects of sewage effluent.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1999C","usgsCitation":"Cable, L.W., Daniel, J.F., Wolf, R.J., and Tate, C.H., 1971, Water resources of the upper White River basin, east-central Indiana: U.S. Geological Survey Water Supply Paper 1999, Report: v, 38 p.; 4 Plates: 25.00 × 20.50 inches or smaller, https://doi.org/10.3133/wsp1999C.","productDescription":"Report: v, 38 p.; 4 Plates: 25.00 × 20.50 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"links":[{"id":25397,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1999c/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":409195,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25547.htm","linkFileType":{"id":5,"text":"html"}},{"id":25395,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999c/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25394,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999c/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25396,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999c/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25393,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999c/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138031,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1999c/report-thumb.jpg"}],"country":"United States","state":"Indiana","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -84.8529052734375,\n 40.233411907115055\n ],\n [\n -84.9737548828125,\n 40.26695230509781\n ],\n [\n -85.0836181640625,\n 40.26695230509781\n ],\n [\n -85.14404296875,\n 40.27533480732468\n ],\n [\n -85.1824951171875,\n 40.29209669470101\n ],\n [\n -85.2264404296875,\n 40.36747374615593\n ],\n [\n -85.3143310546875,\n 40.451127265872316\n ],\n [\n -85.39672851562499,\n 40.49709237269567\n ],\n [\n -85.4461669921875,\n 40.559721346848406\n ],\n [\n -85.616455078125,\n 40.60561205826018\n ],\n [\n -85.836181640625,\n 40.6639728763869\n ],\n [\n -86.011962890625,\n 40.65147128144057\n ],\n [\n -86.33056640625,\n 40.64730356252251\n ],\n [\n -86.407470703125,\n 40.49709237269567\n ],\n [\n -86.4019775390625,\n 40.38002840251183\n ],\n [\n -86.429443359375,\n 40.22921818870117\n ],\n [\n -86.5283203125,\n 40.13269100586688\n ],\n [\n -86.4898681640625,\n 39.97291055131899\n ],\n [\n -86.45690917968749,\n 39.88023492849342\n ],\n [\n -86.45690917968749,\n 39.70296052957233\n ],\n [\n -86.5283203125,\n 39.57182223734374\n ],\n [\n -86.583251953125,\n 39.38950933076637\n ],\n [\n -86.41845703124999,\n 39.308800296002914\n ],\n [\n -86.2371826171875,\n 39.38950933076637\n ],\n [\n -86.1383056640625,\n 39.436192999314095\n ],\n [\n -86.1383056640625,\n 39.56758783088903\n ],\n [\n -86.1053466796875,\n 39.614152077002636\n ],\n [\n -85.924072265625,\n 39.740986355883564\n ],\n [\n -85.8197021484375,\n 39.80009595634841\n ],\n [\n -85.6658935546875,\n 39.863371338285305\n ],\n [\n -85.49560546875,\n 39.918162846609455\n ],\n [\n -85.3912353515625,\n 40.0360265298117\n ],\n [\n -85.2593994140625,\n 40.052847601823984\n ],\n [\n -84.90234375,\n 40.04443758460859\n ],\n [\n -84.8419189453125,\n 40.065460682065535\n ],\n [\n -84.8529052734375,\n 40.233411907115055\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e47e5e4b07f02db4bb69f","contributors":{"authors":[{"text":"Cable, L. W.","contributorId":82677,"corporation":false,"usgs":true,"family":"Cable","given":"L.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":142866,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Daniel, J. F.","contributorId":74357,"corporation":false,"usgs":true,"family":"Daniel","given":"J.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":142865,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wolf, R. J.","contributorId":21518,"corporation":false,"usgs":true,"family":"Wolf","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":142864,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Tate, C. H.","contributorId":93464,"corporation":false,"usgs":true,"family":"Tate","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":142867,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":20895,"text":"ofr71257 - 1971 - A heavy mineral study of Pleistocene and Holocene sediments near Nome, Alaska","interactions":[],"lastModifiedDate":"2024-02-02T21:00:58.594447","indexId":"ofr71257","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"71-257","title":"A heavy mineral study of Pleistocene and Holocene sediments near Nome, Alaska","docAbstract":"A heavy mineral study was carried out for sand-size fractions of onshore Holocene sediments (modern beach and river sediments), nearshore Holocene and Pleistocene relict sediments, and Pleistocene and Pliocene sediments from several nearshore drill-holes. Heavy mineral assemblages of these sediments are dominated by garnet, chlorite, epidote, chloritoid, sphene, and staurolite.
The nearshore region of Nome is mainly underlain by various types of Pleistocene sediments such as relict gravel that Mantles glacial drift, relict gravel over Nome River outwash fan, relict gravelly sand of submerged beaches, and relict gravel that mantles bedrock. In places these relict sediments are covered by Holocene sandy and muddy sediments. The high concentration of heavy minerals is expected for various relict sediments, because the latter were winnowed by several transgressions and regressions of the sea during Pleistocene time. Concentration of heavy minerals, however, is greater for Holocene sand than relict gravel, which mantles glacial drift and relict gravelly sand of submerged beaches. The high concentration of heavy minerals in Holocene sand suggests the winnowing of sand by strong bottom currents. The low concentration of heavy minerals in the relict gravel on glacial drift and relict gravelly sand of submerged beaches is probably due to the heterogenous nature of relict sediments. Sand fractions of the relict sediments probably have been introduced during the Holocene time. Also, contamination of samples of relict gravel from underlying glacial drift is suspected.
A greater concentration of coarse gold particles (1 iiuii. or larger) is found in nearshore relict gravel that mantles glacial drift than in any other sediment type. Relict gravel on glacial drift, which carries high gold values, does not show a high concentration of heavy minerals or a high concentration of garnet. Two factors account for the lack of correlation between concentration of gold and the other heavy minerals: (1) contrast between hydraulic properties of the gold particles and other heavy minerals, and (2) the heterogeneous nature of relict sediments. Because of their extremely high specific gravity, coarse gold particles are not moved by longshore currents or bottom currents from relict gravel which mantles glacial drift, whereas the heavy minerals which are mostly medium to fine sand in size, are transported by longshore currents and strong bottom currents. The Holocene sand winnowed by strong bottom currents shows a high concentration of heavy minerals.
Heavy mineral assemblages are more or less similar for the various sediments. Minor compositional variations mainly reflect the effect of sorting of mineral grains according to size and specific gravity. The frequencies of garnet and staurolite are slightly higher than average for modern beach and river sediments. In nearshore sediments, garnet is most abundant in Holocene sand winnowed by strong bottom currents. Holocene silty sediment which occurs in small patches is characterized by high concentration of micaceous minerals and low concentration of garnet, because the weak currents which deposit fine sediments usually carry light micaceous minerals in great abundance and minerals of high specific gravity like garnet in small amounts. Samples of Pleistocene glacial till and Pliocene marine silt from several nearshore drill-hole locations show high concentrations of micaceous minerals and low concentration of garnet.
Holocene, Pleistocene, and Pliocene sediments of Nome are mostly derived from the same general metamorphic source rocks of the inland region. The majority of the minerals found in heavy mineral assemblages, such as garnet, chlorite, epidote, chloritoid, sphene, staurolite, hornblende, and tremolite-actinolite, are reported to occur in the metamorphic rocks of Nome and the adjacent region.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr71257","usgsCitation":"Sheth, M., 1971, A heavy mineral study of Pleistocene and Holocene sediments near Nome, Alaska: U.S. Geological Survey Open-File Report 71-257, xiii, 83 p., https://doi.org/10.3133/ofr71257.","productDescription":"xiii, 83 p.","costCenters":[],"links":[{"id":425330,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0257/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":153557,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0257/report-thumb.jpg"}],"country":"United States","state":"Alaska","city":"Nome","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -165.46944230357468,\n 64.51990788878058\n ],\n [\n -165.46944230357468,\n 64.48799257721126\n ],\n [\n -165.34584925658916,\n 64.48799257721126\n ],\n [\n -165.34584925658916,\n 64.51990788878058\n ],\n [\n -165.46944230357468,\n 64.51990788878058\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b24e4b07f02db6ae4c5","contributors":{"authors":[{"text":"Sheth, Madhusudan","contributorId":23014,"corporation":false,"usgs":true,"family":"Sheth","given":"Madhusudan","email":"","affiliations":[],"preferred":false,"id":183455,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":22507,"text":"ofr7241 - 1971 - Mathematical ground-water model of Indian Wells Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:08:07","indexId":"ofr7241","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"72-41","title":"Mathematical ground-water model of Indian Wells Valley, California","docAbstract":"A mathematical model of the Indian Wells Valley ground-water basin was developed and verified. The alternating-direction implicit method was used to compute the mathematical solution. It was assumed that there are only two aquifers in the valley, one being deep and the other shallow. Where the shallow aquifer occurs, the underlying deep aquifer is confined or artesian. Flow between the aquifers under steady-state conditions is assumed to be in one direction, from deep to shallow. The transmissivity of the deep aquifer ranges from about 250,000 to 22,000 gallons per day per foot and from about 25,000 to 5,000 gallons per day per foot for the shallow aquifer. The storage coefficient for the deep aquifer ranges from 1 x 10 -4 to 0.20. \r\n\r\nSteady-state recharge and discharge in each aquifer was estimated to be 9,850 acre-feet per year. Ground-water pumping, sewage-effluent recharge, and capture of ground-water discharge occurred under non-steady-state conditions. Most of the ground-water pumpage is near Ridgecrest and Inyokern and in the area between the two towns. By 1968 pumpage in the deep aquifer had caused a reversal in the ground-water gradient south of China Lake and small water-level declines over most of the aquifer. The model for the deep aquifer was verified under steady-state and non-steady-state conditions. The shallow aquifer was verified under steady-state conditions only. \r\n\r\nThe verified model was then used to generate 1983 water-level conditions in the deep aquifer.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey, Water Resources Division,","doi":"10.3133/ofr7241","issn":"0094-9140","usgsCitation":"Bloyd, R., and Robson, S.G., 1971, Mathematical ground-water model of Indian Wells Valley, California: U.S. Geological Survey Open-File Report 72-41, iv, 35 p. :maps ;27 cm., https://doi.org/10.3133/ofr7241.","productDescription":"iv, 35 p. :maps ;27 cm.","costCenters":[],"links":[{"id":156503,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0041/report-thumb.jpg"},{"id":52016,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0041/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52017,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0041/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52018,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0041/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db60ff82","contributors":{"authors":[{"text":"Bloyd, R. M. Jr.","contributorId":73243,"corporation":false,"usgs":true,"family":"Bloyd","given":"R. M.","suffix":"Jr.","affiliations":[],"preferred":false,"id":188371,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Robson, S. G.","contributorId":97102,"corporation":false,"usgs":true,"family":"Robson","given":"S.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":188372,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1339,"text":"wsp1893 - 1971 - Potential development and recharge of ground water in Mill Creek Valley, Butler and Hamilton Counties, Ohio, based on analog model analysis","interactions":[],"lastModifiedDate":"2012-02-02T00:05:13","indexId":"wsp1893","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"1893","title":"Potential development and recharge of ground water in Mill Creek Valley, Butler and Hamilton Counties, Ohio, based on analog model analysis","docAbstract":"Mill Creek valley is part of the greater Cincinnati industrial area in southwestern Ohio. In 1964, nearly 30 percent of the water supply in the study area of about 27 square miles was obtained from wells in the glacial-outwash aquifer underlying the valley. Ground-water demand has increased steadily since the late 1800's, and excessive pumpage during the years of World War II caused water levels to decline to critical levels. Natural recharge to the aquifer, from precipitation, is about 8.5 mgd (million gallons per day). In 1964, the total water use was about 30 mgd, of which 8.1 mgd was obtained from wells in Mill Creek valley, and the remainder was imported from outside the basin. With rapid industrial expansion and population growth, demand for ground water is continuing to increase. By the year 2000 ground-water pumpage is expected to exceed 25 mgd. \r\n\r\nAt a public hearing before the Ohio Water Commission in 1961, artificial recharge of the aquifer through injection wells was proposed as a possible solution to the Mill Creek valley water-supply problem. The present study attempts to determine the feasibility of injection-well recharge systems in the Mill Creek valley. \r\n\r\nAlthough basically simple, the hydrologic system in Mill Creek valley is complex in detail and is difficult to evaluate using conventional quantitative methods. Because of this complexity, an electric analog model was used to test specific development plans. \r\n\r\nThree hypothetical pumping plans were developed by projecting past pumpage data to the years 1980 and 2000. Various combinations of injection wells were tested on the model under different hypothetical conditions of pumpage. Based on analog model analysis, from three to eight inject-ion wells, with an approximate input of 2 mgd each, would reverse the trend in declining groundwater levels and provide adequate water to meet anticipated future demands.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1893","usgsCitation":"Fidler, R.E., 1971, Potential development and recharge of ground water in Mill Creek Valley, Butler and Hamilton Counties, Ohio, based on analog model analysis: U.S. Geological Survey Water Supply Paper 1893, iv, 37 p. :illus., maps. ;23 cm., https://doi.org/10.3133/wsp1893.","productDescription":"iv, 37 p. :illus., maps. ;23 cm.","costCenters":[],"links":[{"id":110030,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25110.htm","linkFileType":{"id":5,"text":"html"},"description":"25110"},{"id":137426,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1893/report-thumb.jpg"},{"id":26399,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1893/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26400,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1893/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26401,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1893/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26402,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1893/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26403,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1893/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db6838f1","contributors":{"authors":[{"text":"Fidler, Richard E.","contributorId":86313,"corporation":false,"usgs":true,"family":"Fidler","given":"Richard","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":143591,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16281,"text":"ofr71284 - 1971 - The Shublik Formation and adjacent strata in northeastern Alaska description, minor elements, depositional environments and diagenesis","interactions":[],"lastModifiedDate":"2012-02-02T00:07:17","indexId":"ofr71284","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"71-284","title":"The Shublik Formation and adjacent strata in northeastern Alaska description, minor elements, depositional environments and diagenesis","docAbstract":"The Shublik Formation (Middle and Late Triassic) is widespread in the surface and subsurface of northern Alaska. Four stratigraphic sections along about 70 miles of the front of the northeastern Brooks Range east of the Canning giver were examined and sampled in detail in 1968. These sections and six-step spectrographic and carbon analyses of the samples combined with other data to provide a preliminary local description of the highly organic unit and of the paleoenvironments. \r\n\r\nThicknesses measured between the overlying Kingak Shale of Jurassic age and the underlying Sadlerochit Formation of Permian and Triassic age range from 400 to more than 800 feet but the 400 feet, obtained from the most completely exposed section, may be closer to the real thickness across the region. The sections consist of organic-rich, phosphatic, and fossiliferous muddy, silty, or carbonate rocks. The general sequence consists, from the bottom up, of a lower unit of phosphatic siltstone, a middle unit of phosphatic carbonate rocks, and an upper unit of shale and carbonate rocks near the Canning River and shale, carbonate rocks, and sandstone to the east.\r\n\r\nAlthough previously designated a basal member of the Kingak Shale (Jurassic), the upper unit is here included with the Shublik on the basis of its regional lithologic relation. \r\n\r\nThe minor element compositions of the samples of the Shublik Formation are consistent with their carbonaceous and phosphatic natures in that relatively large amounts of copper, molybdenum, nickel, vanadium and rare earths are present. The predominantly sandy rocks of the underlying Sadlerochit Formation (Permian and Triassic) have low contents of most minor elements. The compositions of samples of Kingak Shale have a wide range not readily explicable by the nature of the rock: an efflorescent sulfate salt contains 1,500 ppm nickel and 1,500 ppm zinc and large amounts of other metals derived from weathering of pyrite and leaching of local shale. The only recorded occurrence of silver and 300 ppm lead in gouge along a shear plane may be the result of metals introduced from an extraneous source. \r\n\r\nThe deposits reflect a marine environment that deepened somewhat following deposition of the Sadlerochit Formation and then shoaled during deposition of the upper limestone-siltstone unit. This apparently resulted from a moderate transgression and regression of the sea with respect to a northwest-trending line between Barrow and the Brooks Range at the International Boundary. Nearer shore facies appear eastward. The phosphate in nodules, fossil molds and oolites, appears to have formed diagenetically within the uncompacted sediment.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr71284","usgsCitation":"Tourtelot, H.A., and Tailleur, I.L., 1971, The Shublik Formation and adjacent strata in northeastern Alaska description, minor elements, depositional environments and diagenesis: U.S. Geological Survey Open-File Report 71-284, i, 62 leaves :2 folded col. maps ;27 cm., https://doi.org/10.3133/ofr71284.","productDescription":"i, 62 leaves :2 folded col. maps ;27 cm.","costCenters":[],"links":[{"id":150502,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0284/report-thumb.jpg"},{"id":45207,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0284/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45208,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0284/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac6e4b07f02db67a958","contributors":{"authors":[{"text":"Tourtelot, Harry Allison","contributorId":77937,"corporation":false,"usgs":true,"family":"Tourtelot","given":"Harry","email":"","middleInitial":"Allison","affiliations":[],"preferred":false,"id":172546,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tailleur, Irvin L.","contributorId":105304,"corporation":false,"usgs":true,"family":"Tailleur","given":"Irvin","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":172547,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":16250,"text":"ofr71283 - 1971 - The drainage and glacial history of the Still River Valley, southwestern Connecticut","interactions":[],"lastModifiedDate":"2012-02-02T00:07:09","indexId":"ofr71283","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"71-283","title":"The drainage and glacial history of the Still River Valley, southwestern Connecticut","docAbstract":"The Still River is located in southwestern Connecticut. From its origin on the New York border, it passes through Danbury and flows northward to its junction with the Housatonic River in New Milford. \r\n\r\nInterpretation of the Still River's history is based on its surficial geology and bedrock topography. High bedrock surfaces to the south, east, and west of the river show that its preglacial direction was probably to the north. The Still River has developed along the easily eroded Inwood Marble as a subsequent tributary to the Housatonic. \r\n\r\nPleistocene glaciation left a variety of deposits in the Still Valley. The oldest of these is the 'lower' till, of either Illinoian or Altonian age. This till unit is overlain in turn by the Woodfordian 'upper' till. The upper till has basal and ablation facies. Ice-contact deposits formed in the fringing stagnation zone of the last retreating ice sheet. As the glacier withdrew along the Still Valley, preglacial Lake Danbury was impounded against the highlands to the south. Glacial retreat opened progressively lower outlets for this lake. Its final stage was contained by a till (?) barrier at the Housatonic Gorge in New Milford. Filling of the lake by glacial outwash was soon followed by downcutting of the dam and establishment of the modern Housatonic and Still River channels.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr71283","usgsCitation":"Thompson, W.B., 1971, The drainage and glacial history of the Still River Valley, southwestern Connecticut: U.S. Geological Survey Open-File Report 71-283, viii, 55 leaves :ill., 2 maps ;29 cm.; 1 sheet, scale 1:24,000, https://doi.org/10.3133/ofr71283.","productDescription":"viii, 55 leaves :ill., 2 maps ;29 cm.; 1 sheet, scale 1:24,000","costCenters":[],"links":[{"id":148264,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0283/report-thumb.jpg"},{"id":45171,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0283/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45172,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0283/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4d11","contributors":{"authors":[{"text":"Thompson, Woodrow B.","contributorId":67482,"corporation":false,"usgs":true,"family":"Thompson","given":"Woodrow","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":172499,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16152,"text":"ofr71269 - 1971 - Deglaciation events in part of the Manchester South 7.5' quadrangle south-central New Hampshire","interactions":[],"lastModifiedDate":"2018-04-12T15:03:37","indexId":"ofr71269","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"71-269","title":"Deglaciation events in part of the Manchester South 7.5' quadrangle south-central New Hampshire","docAbstract":"The study-area lies in south-central New Hampshire, and is bordered on the west by the Merrimack River, the principal north-south drainage route of central New Hampshire.
The classical two tills of New England outcrop in the area. In a unique exposure of the sandy upper till, a loose ablation unit overlies a compact basal unit. Both upper till facies overlie a sheared section of dense, olive-gray lower till.
Outwash sequences mapped in the study-area are progressively younger to the north, indicating backwastage of the Wisconsinan ice sheet.
Primary structures in proglacial Lake Merrimack sediments include contorted bedding, buckled laminae, and folds. A large slumped section in lake sediments exhibits three distinct deformation zones, characterized by brittle, ductile, and unconsolidated deformation. Cross-cutting relationships establish four fold generations and a deformation sequence in the slumped section. Slip in each fold generation was along nearly parallel slip-lines, as deduced from analyses of fold rotation senses.
The primary and slump deformation features contrast sharply with the intense style of deformation of lake beds below till at an apparent ice readvance cut. The deduced drag fold slip-line agrees with till fabric point maxima and dip-slip on one group of thrust faults. A southerly movement of readvancing ice is inferred.
The study-area was deglaciated about 13,000 years ago, according to a proposed deglaciation model for New Hampshire. The model is based on Nye's theoretical glacier surface gradient, and evidence for active retreat of the Wisconsinan ice sheet.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr71269","usgsCitation":"Stone, B.D., 1971, Deglaciation events in part of the Manchester South 7.5' quadrangle south-central New Hampshire: U.S. Geological Survey Open-File Report 71-269, Report: ix, 84 p.; 2 Sheets: 30.75 x 32.29 inches and 17.76 x 27.37 inches, https://doi.org/10.3133/ofr71269.","productDescription":"Report: ix, 84 p.; 2 Sheets: 30.75 x 32.29 inches and 17.76 x 27.37 inches","costCenters":[],"links":[{"id":45073,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0269/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45074,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0269/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45075,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0269/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":149223,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0269/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db6723d2","contributors":{"authors":[{"text":"Stone, Byron D. 0000-0001-6092-0798 bdstone@usgs.gov","orcid":"https://orcid.org/0000-0001-6092-0798","contributorId":1702,"corporation":false,"usgs":true,"family":"Stone","given":"Byron","email":"bdstone@usgs.gov","middleInitial":"D.","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":172327,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23293,"text":"ofr72157 - 1971 - Hydrologic analysis of Mojave River Basin, California, using electric analog model","interactions":[],"lastModifiedDate":"2012-02-02T00:08:03","indexId":"ofr72157","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"72-157","title":"Hydrologic analysis of Mojave River Basin, California, using electric analog model","docAbstract":"The water needs of the Mojave River basin will increase because of population and industrial growth. The Mojave Water Agency is responsible for providing sufficient water of good quality for the full economic development of the area. The U.S. Geological Survey suggested an electric analog model of the basin as a predictive tool to aid management. \r\n\r\nAbout 1,375 square miles of the alluvial basin was simulated by a passive resistor-capacitor network. The Mojave River, the main source of recharge, was simulated by subdividing the river into 13 reaches, depending on intermittent or perennial flow and on phreatophytes. The water loss to the aquifer was based on records at five gaging stations. The aquifer system depends on river recharge to maintain the water table as most of the ground-water pumping and development is adjacent to the river. \r\n\r\nThe accuracy and reliability of the model was assessed by comparing the water-level changes computed by the model for the period 1930-63 with the changes determined from field data for the same period.\r\n\r\nThe model was used to predict the effects on the physical system by determining basin-wide water-level changes from 1930-2000 under different pumping rates and extremes in flow of the Mojave River. Future pumping was based on the 1960-63 rate, on an increase of 20 percent from this rate, and on population projections to 2000 in the Barstow area. For future predictions, the Mojave River was modeled as average flow based on 1931-65 records and also as high flow, 1937-46, and low flow, 1947-65. \r\n\r\nOther model runs included water-level change 1930-63 assuming aquifer depletion only and no recharge, effects of a well field pumping 10,000 acre-feet in 4 months north of Victorville and southeast of Yermo, and effects of importing 10,000, 35,000, and 50,800 acre-feet of water per year from the California Water Project into the Mojave River for conveyance downstream.","language":"ENGLISH","publisher":"U.S.G.S.,","doi":"10.3133/ofr72157","issn":"0094-9140","usgsCitation":"Hardt, W.F., 1971, Hydrologic analysis of Mojave River Basin, California, using electric analog model: U.S. Geological Survey Open-File Report 72-157, 84 p. :ill., charts, graphs, map [folded in pocket] ;27 cm., https://doi.org/10.3133/ofr72157.","productDescription":"84 p. :ill., charts, graphs, map [folded in pocket] ;27 cm.","costCenters":[],"links":[{"id":156075,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1972/0157/report-thumb.jpg"},{"id":52579,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0157/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52580,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0157/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52581,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0157/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52582,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0157/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":52583,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1972/0157/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db684229","contributors":{"authors":[{"text":"Hardt, W. F.","contributorId":12455,"corporation":false,"usgs":true,"family":"Hardt","given":"W.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":189829,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15295,"text":"ofr71222 - 1971 - Selected fluvial monazite deposits in the southeastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:06:47","indexId":"ofr71222","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"71-222","title":"Selected fluvial monazite deposits in the southeastern United States","docAbstract":"Farther southwest in Georgia, around Griffin and Zebullon, along streams tributary to the Flint River in the monazite belt the flood plains are generally small and discontinuous, and only about 1 percent of the sediment is gravel. The area between Griffin, Zebullon, and the Flint River is underlain by biotite schist and biotite gneiss into which biotite granite has been intruded. Only along one stream, Flat Creek, which drains monazite-bearing granite near Zetella, Ga., are the tenors in monazite even moderately high, but a combination of thick, clayey overburden and discontinuous flood plains make the stream unsuitable for placer mining. Elsewhere in the Flint River area the heavy-mineral concentrates contain less than 1 percent monazite. \r\n\r\nThe southwesternmost area in which reconnaissance of the monazite belt was conducted includes a groups of southwest-flowing tributaries to the Chattahoochee River north of Pine Mountain and near La Grange, Ga. A combination of three characteristics of the alluvium make the area unfavorable for mining: (1) the upper half of the sedimentary sequence is clay and silt, (2) there is scant gravel, and (3) much of the sand is fine grained. Monazite is associated with the Snelson Granite, schists, and gneisses north of the Towaliga fault, but even in this area the tenor of most riffle sediments is only 0.1 to 0.5 pound of monazite per cubic yard, and the average tenor of the alluvium is about 0.2 pound per cubic Yard. Rocks south of the Towaliga fault contain scant monazite. The monazite-bearing area in the drainage basin of the Chattahoochee River has no monazite placers.\r\n\r\nEvidence from the areas on the Flint and Chattahoochee Rivers shows that streams in western Georgia are a much poorer source of monazite than streams farther to the northeast in Georgia, South Carolina, and North Carolina. Also, the northeastern part of the belt in the drainage basins of the Yadkin and Dan Rivers is a poorer source for monazite than the area between the Savannah and Catawba Rivers, S.C.-N.C. \r\n\r\nMonazite-bearing crystalline rocks in the western belt contain about 0.06 pound of monazite per cubic yard. Residual soil derived from the crystalline rocks contains about 0.3 to 0.4 pound of monazite per cubic yard, and colluvial sediments formed by sheet-wash from saprolite, residual soil, and, rarely, old stream deposits, have an average of 3.1 pounds of monazite to the cubic yard. The data on the tenors of residual and colluvial deposits are far less comprehensive than those an the quantity of monazite in the crystalline rocks, but the tenors are probably of the correct order of magnitude. Neither the crystalline rocks nor the residual soils are ores of monazite. Because the colluvial deposits are thin and have patch distribution they could not be mined independently, but some colluvium could be stripped from the adjoining hills in conjunction with the mining of alluvial deposits in the valleys. \r\n\r\nIt is most unlikely that alluvial monazite placers have formed in the trunk streams leading southeastward out of the monazite belt. Churn drilling on the Broad and North Tyger Rivers, South Carolina, at the east edge of the belt has shown that the bulk of the alluvium is fine-grained sediment that contains 0.2 to 0.4 pound of monazite per cubic yard--tenors that represent no considerable enrichment over those in the crystalline rocks and residual soils. The probable persistence of predominantly fine-grained alluvium downstream to the Coastal Plain and the certain dilution of monazite-bearing concentrates by the inflow of monazite-free suites of heavy minerals between the belt and the fall line suggest that the trunk streams east of the belt are the least favorable sources for alluvial monazite in the Piedmont?","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr71222","usgsCitation":"Overstreet, W.C., White, A.M., Theobald, P., and Caldwell, D.W., 1971, Selected fluvial monazite deposits in the southeastern United States: U.S. Geological Survey Open-File Report 71-222, iv, 108 leaves :4 folded maps ;27 cm., https://doi.org/10.3133/ofr71222.","productDescription":"iv, 108 leaves :4 folded maps ;27 cm.","costCenters":[],"links":[{"id":146455,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0222/report-thumb.jpg"},{"id":44219,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44220,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44221,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44222,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0222/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":44223,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1971/0222/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa31c","contributors":{"authors":[{"text":"Overstreet, William C.","contributorId":73586,"corporation":false,"usgs":true,"family":"Overstreet","given":"William","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":170908,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"White, A. M.","contributorId":86778,"corporation":false,"usgs":true,"family":"White","given":"A.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":170909,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Theobald, P. K.","contributorId":45293,"corporation":false,"usgs":true,"family":"Theobald","given":"P. K.","affiliations":[],"preferred":false,"id":170907,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Caldwell, D. W.","contributorId":27461,"corporation":false,"usgs":true,"family":"Caldwell","given":"D.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":170906,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70199680,"text":"70199680 - 1971 - Hydrogeologic characteristics of the valley-fill aquifer in the Arkansas River Valley, Bent County, Colorado","interactions":[],"lastModifiedDate":"2022-05-24T21:55:31.127238","indexId":"70199680","displayToPublicDate":"1984-12-31T10:12:09","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Hydrogeologic characteristics of the valley-fill aquifer in the Arkansas River Valley, Bent County, Colorado","docAbstract":"The investigation on which this report is based is a part of a comprehensive evaluation of the water resources of the Arkansas River valley undertaken by the U.S. Geological Survey in cooperation with the Colorado Water Conservation Board and the Southeastern Colorado Water Conservancy District. The study reach extends 150 miles from Pueblo to the Kansas State line (see fig. 1 index map). The water-resources investigation of the stream aquifer system in the Arkansas River valley, which began in 1963, is being made to provide information about the water resources for planning, management, and administration of the supply.
The objectives of the investigation are to define the effects of present water use, to determine the relation between ground and surface water, and to evaluate the effects of proposed changes in water law and management. The major steps in the study are: (1) Inventory the water resources, (2) describe the hydrogeologic character of the aquifer, (3) document and evaluate the effects of development, (4) construct and verify models to aid in the evaluation of the hydrology, and (5) develop models to test water-management plans and to optimize water use.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/70199680","collaboration":"Prepared in cooperation with the Colorado Water Conservation Board and the Southeastern Colorado Water Conservancy District","usgsCitation":"Hurr, R.T., and Moore, J.E., 1971, Hydrogeologic characteristics of the valley-fill aquifer in the Arkansas River Valley, Bent County, Colorado: Open-File Report, Report: i, 9 p.; 4 Plates: 35.81 x 20.16 inches or less, https://doi.org/10.3133/70199680.","productDescription":"Report: i, 9 p.; 4 Plates: 35.81 x 20.16 inches or less","costCenters":[],"links":[{"id":401019,"rank":8,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15848.htm"},{"id":400998,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70199680/plate-3b.pdf","text":"Plate 3B","linkFileType":{"id":1,"text":"pdf"}},{"id":400999,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70199680/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":357699,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70199680/report-thumb.jpg"},{"id":400994,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70199680/report.pdf"},{"id":400995,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70199680/plate-2a.pdf","text":"Plate 2A","linkFileType":{"id":1,"text":"pdf"}},{"id":400996,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70199680/plate-2b.pdf","text":"Plate 2B","linkFileType":{"id":1,"text":"pdf"}},{"id":400997,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70199680/plate-3a.pdf","text":"Plate 3A","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Colorado","county":"Bent County","otherGeospatial":"Arkansas River Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.38333333333334,38 ], [ -103.38333333333334,38.166666666666664 ], [ -102.75,38.166666666666664 ], [ -102.75,38 ], [ -103.38333333333334,38 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hurr, R. Theodore","contributorId":27023,"corporation":false,"usgs":true,"family":"Hurr","given":"R.","email":"","middleInitial":"Theodore","affiliations":[],"preferred":false,"id":746173,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moore, John E.","contributorId":33688,"corporation":false,"usgs":true,"family":"Moore","given":"John","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":746174,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70198177,"text":"70198177 - 1971 - Impact breccias in carbonate rocks, Sierra Madera, Texas","interactions":[],"lastModifiedDate":"2018-07-19T09:49:59","indexId":"70198177","displayToPublicDate":"1971-12-31T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Impact breccias in carbonate rocks, Sierra Madera, Texas","docAbstract":"Two main types of deformational breccia occur in the Sierra Madera cryptoexplosion structure: monolithologic breccias composed of shattered rock of a single lithology and mixed breccias composed of rocks of several lithologies. Monolithologic breccias generally show no mineralogic signs of shock deformation, but a few samples are shatter-coned in a manner suggesting simultaneous formation of breccias and shatter cones. Mixed breccias, forming irregular, cross-cutting bodies, consistently contain moderately to highly shocked material, with mineralogic evidence of shock pressures of 50 kb to more than 200 kb, which, with evidence from the structural geometry of Sierra Madera and orientation of shatter cones, indicate an impact origin of the breccias.
The mode of occurrence of the breccias, petrographic characteristics, and association with shock features are shared by breccias in many other cryptoexplosion structures in both carbonate and crystalline rock terranes, suggesting that such breccias have a common origin.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1971)82[1009:IBICRS]2.0.CO;2","usgsCitation":"Wilshire, H.G., Howard, K.A., and Offield, T., 1971, Impact breccias in carbonate rocks, Sierra Madera, Texas: GSA Bulletin, v. 82, no. 4, p. 1009-1018, https://doi.org/10.1130/0016-7606(1971)82[1009:IBICRS]2.0.CO;2.","productDescription":"10 p.","startPage":"1009","endPage":"1018","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":355802,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Texas","otherGeospatial":"Sierra Madera crater","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -104.205322265625,\n 30.002516938570686\n ],\n [\n -102.19482421875,\n 30.002516938570686\n ],\n [\n -102.19482421875,\n 31.784216884487385\n ],\n [\n -104.205322265625,\n 31.784216884487385\n ],\n [\n -104.205322265625,\n 30.002516938570686\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"82","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Wilshire, H. G.","contributorId":36125,"corporation":false,"usgs":false,"family":"Wilshire","given":"H.","middleInitial":"G.","affiliations":[],"preferred":false,"id":740433,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Howard, Keith A. 0000-0002-6462-2947 khoward@usgs.gov","orcid":"https://orcid.org/0000-0002-6462-2947","contributorId":3439,"corporation":false,"usgs":true,"family":"Howard","given":"Keith","email":"khoward@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":740434,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Offield, Terry W.","contributorId":64217,"corporation":false,"usgs":true,"family":"Offield","given":"Terry W.","affiliations":[],"preferred":false,"id":740435,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70227386,"text":"70227386 - 1971 - Tertiary igneous chronology of the Great Basin of western United States — Implications for tectonic models","interactions":[],"lastModifiedDate":"2022-01-12T18:51:08.206116","indexId":"70227386","displayToPublicDate":"1971-12-01T12:42:35","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Tertiary igneous chronology of the Great Basin of western United States — Implications for tectonic models","docAbstract":"The chronology of igneous activity in the Great Basin of western United States is used as a time framework for a simple plate model. This chronology suggests that a plate (Farallon plate) became underthrust to sufficient depth by the middle Tertiary to trigger the eruption of volcanic rocks of andesitic to rhyolitic composition in the central part of the Great Basin, 40 m.y. ago. This plate continued to be underthrust until about 19 m.y. ago, at which time it was completely consumed and volcanic activity ceased. When the oceanic ridge reached a certain point under the Great Basin about 16 m.y. ago, this resulted in the widespread eruption of olivine basalt and the main initial phase of Basin and Range faulting.
Quantitative estimates of ground-water pumpage from the principal ground-water basins in California are necessary for future appraisal studies, for constructing hydrologic models, and for systematic planning of water use and conservation. Methods of estimating pumpage for this report are based on metered pumpages, on electric-power consumption and fuel consumption by internal-combustion engines or agricultural wells, and on duty of water for municipal areas. This report is the third of a series planned to include the Central Valley of California.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/70260852","collaboration":"Prepared in cooperation with the California Department of Water Resources","usgsCitation":"Mitten, H.T., and Ogilbee, W., 1971, Ground-water pumpage in parts of Merced, Madera, Fresno, Kings, and Tulare Counties, California, 1962-66: Open-File Report, iii, 8 p., https://doi.org/10.3133/70260852.","productDescription":"iii, 8 p.","costCenters":[],"links":[{"id":463876,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70260852/report-thumb.jpg"},{"id":485009,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70260852/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"California","county":"Fresno County, Madera County, Merced County, Tulare County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.74265624125817,\n 37.42406923520494\n ],\n [\n -121.74265624125817,\n 35.85671302602901\n ],\n [\n -118.12127194447606,\n 35.85671302602901\n ],\n [\n -118.12127194447606,\n 37.42406923520494\n ],\n [\n -121.74265624125817,\n 37.42406923520494\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Mitten, Hugh T.","contributorId":103652,"corporation":false,"usgs":true,"family":"Mitten","given":"Hugh","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":918299,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ogilbee, William","contributorId":106093,"corporation":false,"usgs":true,"family":"Ogilbee","given":"William","email":"","affiliations":[],"preferred":false,"id":918300,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70227354,"text":"70227354 - 1971 - Tectonics of the Mendocino triple junction","interactions":[],"lastModifiedDate":"2022-01-10T23:11:46.320538","indexId":"70227354","displayToPublicDate":"1971-11-01T17:03:40","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Tectonics of the Mendocino triple junction","docAbstract":"Interpretation of reflection profiles and of the magnetic anomaly pattern over the Gorda Basin and Escarpment gives broad agreement with the triple junction model of McKenzie and Morgan (1969). However, the basin has undergone internal deformation, a local departure from rigid plate tectonics, and the escarpment has had a component of underthrusting by the Gorda block. Faults in the Gorda Basin which disturb young turbidites parallel the trends of magnetic anomalies, suggesting deformation of the oceanic crust along lines of primary weakness. The northeast trends of the faults give a constraint on first-motion solutions for earthquakes within the basin and suggest left-lateral slip on the faults. Analysis of the geometry and timing of the Gorda Basin deformation based on the magnetic pattern gives an average gross tectonic strain rate of 10−14/sec. These observations give a measure of the mechanics of deformation of oceanic lithosphere very close to a spreading rise crest.
The normal balance between fresh water in coastal aquifers and sea water applies also to carbonate-rock aquifers that have been karstified, but there are local modifications in the balance that need to be considered. Uneven distribution of permeability, expressed by a network of solution channels bounded by relatively impermeabler rock, causes an uneven distribution of head of the environmental water along the seacoast. Where sinkholes and (or) vertical solution shafts below sea level penetrate the aquifer, the fresh ground water may discharge through these karst features if the fresh-water head is greater than that of the salt water. However, under some conditions the salt-water head may exceed that of the fresh water, and the direction of movement is reversed as sea water flows into the aquifer. This sea-water flow into the aquifer occurs (1) where sinkholes, acting as “cased wells,” penetrate less permeable rock before reaching a lateral solution channel and (2) where (or when) the fresh-water head is less than that required to balance the salt water. On Andros Island, Bahamas, the range in tide (as much as 5 feet) from low tide to high tide is sufficient to cause such a reversal locally. During low tide the salt-water head becomes sufficiently low that the ground-water head exceeds that of the sea water, and the ground water flows through the sinkholes to the ocean floor; during high tide sea water flows in the sinkholes. In the Adriatic Sea along the coast of Yugoslavia, apparently the fresh-water head is sufficient to produce perennial springs in some localities, but in other areas, as in the Bay of Kastela near Split, the fresh-water head becomes low enough during some seasons that the flow is reversed and salt water enters the aquifer through the karst features.
The development of sinkholes and other karst features near the present coast and extending below sea level occurred generally during a low stand of the Pleistocene sea when the top of the saturated zone stood lower than the bottom of the deepest sinkholes or natural wells.
Integrated evaluations of (1) the distribution of permeability in coastal karst regions and (2) the principles relating to the dynamic balance between fresh aquifer water and sea water are leading to better knowledge of methods that may salvage much karst water which is lost to the sea.
Some roll-type uranium deposits are marginal to an altered tongue in sandstone beds that originally contained more-or-less uniformly distributed pyrite. Mineralizing solutions percolated through the sandstone, oxidized nearly all the pre-existing pyrite, and then redeposited part of the pyrite downstream in an embryonic ore zone. The pyrite and the entire ore zone continued to migrate downstream in the sandstone, much as a sand dune migrates. The amount of pyrite in mature deposits varies systematically with the position in the ore body. It is postulated that the rate at which the pyrite was redeposited controlled the systematic variation in distribution of pyrite.Biogenic and chemical models which are described in the literature provide alternate explanations for the genesis of roll-type uranium deposits in sandstone. The different theoretical rates for the precipitation of pyrite in the two genetic models provide a distinctive distribution of pyrite that characterizes each process. The theoretical difference between the biogenic and chemical models provides a mathematical technique for identifying the origin of a deposit. Mathematical analysis of the pyrite content of a uranium deposit in the Shirley Basin, Wyoming, illustrates a practical application of the theory. Although a definite conclusion about the origin of roll-type deposits would require considerably more data than are now available, the pyrite content of this deposit does correspond to the theoretical pyrite content of the chemical model, suggesting that a disproportionation reaction was involved in its formation.
The effect of salinity on the temperature-depth relations of a brine of constant composition, enclosed in a vein system, but freely connected to the surface, and everywhere at the boiling point for the hydrostatic head, was calculated by using a mathematical model. The Na-Ca-K-Cl brines which are found in thermal springs and in fluid inclusions in ore minerals were approximated by the available data for vapor-saturated NaCl-H2O solutions. In general, the results are similar to those calculated by D. E. White in 1968 for H 2 O, except that the gradients are steeper because of the increase in density and the decrease in vapor pressure caused by the dissolved salt. As a practical rule, the depth to an isotherm in a 5, 10, 15, 20, and 25 wt percent NaCl brine system is, respectively, 92, 84, 77, 70, and 63 percent (+ or -2 percent) of the depth to the same isotherm in an H2O system. From the data presented, the minimum depth to the growth site of crystals containing fluid inclusions which indicate boiling of the brine can be estimated. Among other applications, these results are useful toward the understanding of the behavior of brines in geothermal areas which may or may not contain compositional stratification.
Interest in the geochemistry of groundwater is increasing owing to the great number of current projects involving underground liquid waste storage, artificial recharge of potable water, accidental contamination of groundwater bodies, sanitary landfills, and pollution monitoring. Geochemical techniques used to facilitate the understanding of a groundwater system range from extremely simple to those requiring sophisticated theories, equipment, and procedures. An interpretation of the simple trilinear diagram for samples collected from the Yucatan Peninsula of Mexico provided evidence that the fresh-water body was only a few tens of meters thick and was underlain everywhere by an extensive body of salt water. A geochemical technique that has been used effectively to identify the source of salt water in coastal aquifers is measurement of the carbon-14 concentrations. Carbon-14 has been used in a regional carbonate aquifer to determine the velocity of groundwater movement, rates of chemical reactions, and distribution of hydraulic conductivity. The application of principles of irreversible thermodynamics to groundwater systems provides a basis for constructing models which permit prediction, over both time and space, of changes in head distribution and chemical character of the water resulting from imposed stresses on the system. In essence, proper application of irreversible thermodynamics combines the potential theory of Hubbert with principles of reversible chemical thermodynamics, such as solution of carbonate minerals, to describe and explain controlling chemical reactions and processes of groundwater systems.
The relationship between the gravitational and magnetic potentials caused by a uniform distribution of mass and magnetization may be used to obtain independent information about these physical properties. The general relationship in the frequency domain between the Fourier transforms of the gravity and magnetic anomaly fields is established through the Poisson theorem. The discrete Fourier transforms of the sampled continuous functions are used in an analysis which leads to a system of linear equations involving terms in density, magnetization, and calculated finite Fourier-series coefficients. A least squares solution of the system yields the three components of the total magnetization vector divided by the density. From these results, the direction of total magnetization and the minimum of the Koenigsberger ratio Q can be determined uniquely. The remanent magnetization direction and certain other information can be derived for special cases in which the value of one or more of the physical property terms can be assigned. Accurate results were obtained in the analysis of data from a theoretical model. Analysis of gravity and magnetic data from the North Atlantic Gilliss seamount indicates the presence of a significant component of remanent magnetization and leads to derived physical properties which are in fairly close agreement with dredged sample data. The calculated direction of remanent magnetization indicates a paleomagnetic pole position in eastern Siberia, in general agreement with the predicted position for a Cretaceous source in the North Atlantic. The seamount example illustrates certain contingent problems to be considered in practical application of the method.
The Apollo 14 lunar module landed in a region of the lunar highlands that is part of a widespread blanket of ejecta surrounding the Mare Imbrium basin. Samples were collected from the regolith developed on a nearly level plain, a ridge 100 meters high, and a blocky ejecta deposit around a young crater. Large boulders in the vicinity of the landing site are coherent fragmental rocks as are some of the returned samples.
","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.173.3998.716","issn":"00368075","usgsCitation":"Swann, G., Trask, N., Hait, M., and Sutton, R.L., 1971, Geologic setting of the Apollo 14 samples: Science, v. 173, no. 3998, p. 716-719, https://doi.org/10.1126/science.173.3998.716.","productDescription":"4 p.","startPage":"716","endPage":"719","costCenters":[],"links":[{"id":219228,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"173","issue":"3998","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a21dde4b0c8380cd56b5b","contributors":{"authors":[{"text":"Swann, G.A.","contributorId":8859,"corporation":false,"usgs":true,"family":"Swann","given":"G.A.","email":"","affiliations":[],"preferred":false,"id":358688,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Trask, N.J.","contributorId":31729,"corporation":false,"usgs":true,"family":"Trask","given":"N.J.","email":"","affiliations":[],"preferred":false,"id":358690,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hait, M. H.","contributorId":59052,"corporation":false,"usgs":true,"family":"Hait","given":"M. H.","affiliations":[],"preferred":false,"id":358691,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Sutton, R. L.","contributorId":24364,"corporation":false,"usgs":true,"family":"Sutton","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":358689,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70227137,"text":"70227137 - 1971 - Tertiary limestone aquifer system in the southeastern states","interactions":[],"lastModifiedDate":"2021-12-30T18:49:08.037353","indexId":"70227137","displayToPublicDate":"1971-08-01T12:36:14","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Tertiary limestone aquifer system in the southeastern states","docAbstract":"The hydrogeologic history of the Tertiary limestone system of the Southeastern States is reconstructed, especially as it relates to circulation of ground water and the development of solution cavities. The development of these solution cavities resembles in many respects the development of cavities in carbonates of the Knox Group of Tennessee during Middle Ordovician time, the cavities in the Knox having since been filled with collapse breccia that has been recemented. Some general principles of the circulation of water in limestone terranes and the related development of solution openings are reviewed so that a generic basis for comparison can be made of the modern southeast carbonate setting with the Ordovician carbonate setting in Tennessee.The major requirements for solutional development as cavities--(1) presence of highly soluble material, (2) a fracture system or some other form of incipient permeability, (3) water undersaturated with respect to soluble rocks, such as recharge from precipitation, and (4) hydraulic gradient--are found in the Tertiary limestone terrane of the southeast; much of the limestone has been elevated above sea level as a homoclinal seaward-dipping unit. Such a broad homoclinal setting, which also existed in the Knox at the close of early Ordovician time, facilitates extensive solutional development in the upper part of the zone of saturation. Circulation of water great enough to form a significant cavern network requires concentrated discharge areas, commonly as entrenched permanent streams or near-shore springs and seepage. This condition prevails where the Tertiary limestone is fairly close to land surface.Reconstruction of the geologic and hydrogeologic history of a carbonate region generally reveals the extent of early solution and karst development in relation to current karstification. Caverns, partly filled in some cases with loose or poorly cemented rock fragments that have fallen from cavern roofs, give evidence of karstification that is either current or that probably developed since the last marine inundation of the carbonate terrane. On the other hand, filling of caverns with overlying rock debris and reconstituting the debris into breccia are conditions that require evaluation of paleohydrology.