This map is intended as a guide for those who enjoy outdoor recreation in magnificent scenic settings.
The Salina quadrangle lies in the heart of the Colorado Plateau, a sparsely populated land of unique and outstanding scenic beauty. The eastern half of the quadrangle is a great desert, partly blanketed by sand dunes, but mostly an area of badlands multicolored cliffs and benches of virtually barren rock, and deeply incised canyons. In the west half of the quadrangle, rugged tree-covered foothills flank high forested plateaus rimmed by cliffs. On these High Plateaus, dense coniferous forest is interspersed with wide grassy parks, grazed in summer by sheep and cattle. Valleys between the plateaus contain irrigated crop lands.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Geology, structure, and uranium deposits of the Salina quadrangle, Utah","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/i591O","usgsCitation":"Williams, P., and Covington, H., 1973, Map showing scenic features and recreation facilities in the Salina quadrangle, Utah: U.S. Geological Survey IMAP 591, 1 Plate: 39.86 x 27.64 inches, https://doi.org/10.3133/i591O.","productDescription":"1 Plate: 39.86 x 27.64 inches","costCenters":[],"links":[{"id":493516,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_9388.htm","linkFileType":{"id":5,"text":"html"}},{"id":256595,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/imap/0591o/report-thumb.jpg"},{"id":256593,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/imap/0591o/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":256594,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/imap/0591o/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"250000","country":"United States","state":"Utah","otherGeospatial":"Salina quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112,38 ], [ -112,39 ], [ -110,39 ], [ -110,38 ], [ -112,38 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b13e4b07f02db6a32ea","contributors":{"authors":[{"text":"Williams, Paul L.","contributorId":181839,"corporation":false,"usgs":false,"family":"Williams","given":"Paul L.","affiliations":[],"preferred":false,"id":276134,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Covington, Harry R.","contributorId":101309,"corporation":false,"usgs":true,"family":"Covington","given":"Harry R.","affiliations":[],"preferred":false,"id":276135,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":204,"text":"wsp2092 - 1973 - Quality of surface waters of the United States, 1968, Part 2, South Atlantic slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:11","indexId":"wsp2092","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"2092","title":"Quality of surface waters of the United States, 1968, Part 2, South Atlantic slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp2092","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1973, Quality of surface waters of the United States, 1968, Part 2, South Atlantic slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 2092, x, 373 p. ;23 cm., https://doi.org/10.3133/wsp2092.","productDescription":"x, 373 p. ;23 cm.","costCenters":[],"links":[{"id":135999,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2092/report-thumb.jpg"},{"id":24815,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2092/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db651958","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":527233,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23751,"text":"ofr741064 - 1973 - Preliminary investigation of land subsidence in the Sacramento Valley, California","interactions":[],"lastModifiedDate":"2025-07-25T17:07:11.89918","indexId":"ofr741064","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"74-1064","title":"Preliminary investigation of land subsidence in the Sacramento Valley, California","docAbstract":"Although a number of agencies have made leveling surveys in Sacramento Valley and a valleywide network of first- and second-order control exists, few areas have sufficient control for determining whether land subsidence has occurred and if so, how much, within the time span of vertical control. Available data suggest that 0.2 to 0.9 foot (0.06 to 0.3 m) of subsidence probably has occurred from 1935-42 to 1964 in an extensive agricultural area of heavy ground-water pumping between Zamora and Davis, and that as much as 2 feet (0.6 m) of subsidence has occurred in at least two areas of pumping overdraft--east of Zamora, and west of Arbuckle. \r\n\r\nA comparison of maps showing long-term water-level decline and average annual ground-water pumpage indicates several other areas of probable subsidence. In six general areas--northwest of Sacramento; northeast of Sacramento; southeast of Yuba City; 10 miles (16 km) north of Willows; 20 miles (32 km) north of Willows; and especially in the Arbuckle area,ground-water declines have quite probably produced significant subsidence. In two areas of most intensive pumping, no long-term water-level declines have occurred, and no subsidence is indicated.\r\n\r\nIf problems of land subsidence are of concern in Sacramento Valley, and if estimates of historic subsidence or subsidence potential are needed, serious consideration should be given to a field program of basic-data collection. Second-order leveling along a few carefully selected lines of existing control, and the installation and operation of two or three compaction recorders in areas of continuing water-level decline, would provide helpful data for estimating .past and future subsidence.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr741064","issn":"0094-9140","usgsCitation":"Lofgren, B.E., and Ireland, R.L., 1973, Preliminary investigation of land subsidence in the Sacramento Valley, California: U.S. Geological Survey Open-File Report 74-1064, Report: 32 p.; 4 Figures: 17.20 x 22.10 inches or smaller, https://doi.org/10.3133/ofr741064.","productDescription":"Report: 32 p.; 4 Figures: 17.20 x 22.10 inches or smaller","costCenters":[],"links":[{"id":492916,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1974/1064/figure-4.pdf","text":"Figure 4","linkFileType":{"id":1,"text":"pdf"}},{"id":492915,"rank":6,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1974/1064/figure-3.pdf","text":"Figure 3","linkFileType":{"id":1,"text":"pdf"}},{"id":492914,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1974/1064/figure-2.pdf","text":"Figure 2","linkFileType":{"id":1,"text":"pdf"}},{"id":492913,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1974/1064/figure-1.pdf","text":"Figure 1","linkFileType":{"id":1,"text":"pdf"}},{"id":52984,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1974/1064/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":391027,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_52091.htm"},{"id":156134,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1974/1064/report-thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Sacramento Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.5,\n 38.5\n ],\n [\n -121.1667,\n 38.5\n ],\n [\n -121.1667,\n 40.5833\n ],\n [\n -122.5,\n 40.5833\n ],\n [\n -122.5,\n 38.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aabe4b07f02db669e77","contributors":{"authors":[{"text":"Lofgren, B. E.","contributorId":42579,"corporation":false,"usgs":true,"family":"Lofgren","given":"B.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":190653,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ireland, R. L.","contributorId":89893,"corporation":false,"usgs":true,"family":"Ireland","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":190654,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":24797,"text":"ofr73358 - 1973 - Artificial recharge in the Waterman Canyon-East Twin Creek area, San Bernardino County, California","interactions":[],"lastModifiedDate":"2012-02-02T00:08:17","indexId":"ofr73358","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-358","title":"Artificial recharge in the Waterman Canyon-East Twin Creek area, San Bernardino County, California","docAbstract":"This is a study of the feasibility of recharging, in the Waterman Canyon-East Twin Creek area, imported water from northern California by way of the State Water Project beginning in 1972. \r\n\r\nThe feasibility of recharging 30,000 acre-feet of water a year in the Waterman Canyon-East Twin Creek area will depend on the effectiveness of fault K as a barrier to ground-water movement near the land surface. The results of test drilling and an infiltration test indicate that the subsurface material at the spreading grounds is permeable enough to allow recharged water to percolate to the water table. The data indicate that fault K extends into the Waterman Canyon-East Twin Creek area and may impede the lateral movement of recharged water. Fault K has no known surface expression and therefore probably does not affect the highly permeable younger alluvium. If that is so, fault K will be less effective as a barrier to ground-water movement as the recharge mound rises. Monitoring of the observation wells near the spreading grounds as the planned recharge operation proceeds should provide data about the hydrologic effects of fault K near the land surface.","language":"ENGLISH","publisher":"U.S. Geological Survey, Water Resources Division,","doi":"10.3133/ofr73358","issn":"0094-9140","usgsCitation":"Warner, J.W., and Moreland, J.A., 1973, Artificial recharge in the Waterman Canyon-East Twin Creek area, San Bernardino County, California: U.S. Geological Survey Open-File Report 73-358, iv, 44 p. :ill., maps ;27 cm., https://doi.org/10.3133/ofr73358.","productDescription":"iv, 44 p. :ill., maps ;27 cm.","costCenters":[],"links":[{"id":157510,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0358/report-thumb.jpg"},{"id":53810,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0358/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":53811,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0358/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abbe4b07f02db672c47","contributors":{"authors":[{"text":"Warner, J. W.","contributorId":42996,"corporation":false,"usgs":true,"family":"Warner","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":192582,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moreland, J. A.","contributorId":71994,"corporation":false,"usgs":true,"family":"Moreland","given":"J.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":192583,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2406,"text":"wsp2006 - 1973 - The Pine-Popple River basin — Hydrology of a wild river area, northeastern Wisconsin","interactions":[],"lastModifiedDate":"2022-12-01T19:23:30.261504","indexId":"wsp2006","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"2006","title":"The Pine-Popple River basin — Hydrology of a wild river area, northeastern Wisconsin","docAbstract":"The Pine and Popple Rivers, virtually unaltered by man, flow through a semiprimitive area of forests, lakes, and glacial hills. White-water streams, natural lakes, fish and animal life, and abundant vegetation contribute to the unique recreational and aesthetic characteristics of the area. Resource planning or development should recognize the interrelationships within the hydrologic system and the possible effects of water and land-use changes upon the wild nature of the area. The basin covers about 563 square miles in northeastern Wisconsin. Swamps and wetlands cover nearly 110 square miles, and the 70 lakes cover about 11 square miles. The undulating topography is formed by glacial deposits overlying an irregular, resistant surface of bedrock. An annual average of 30 inches of precipitation, highest from late spring to early autumn, falls on the basin. Of this amount, evapotranspiration, highest in mid summer and late summer, averages 19 inches; the remaining 11 inches is runoff, which is highest in spring and early summer. Ground water from the glacial drift is the source of water for the minor withdrawal use in the basin. Ground-water movement is to streams and lakes and regionally follows the slope of topography and the bedrock surface, which is generally west to east. Ground water is of good quality, although locally high in iron. The major uses of water are for recreation and power generation. Domestic use is slight. No water is withdrawn from lakes or streams, and no sewage or industrial wastes are added to lakes or streams. Most of the flow of the Pine River is used for power generation. The main stems of the Pine and Popple Rivers contain 114 canoeable miles, of which 95 percent is without such major obstructions as falls or large rapids. In general streams support cold-water fish, and lakes support warm-water fish. Trout is the principal stream and game fish in the basin. The basin has no significant water problems. Future development between the Pine River power plant and the mouth of the Pine River should have little effect on the western two-thirds of the basin, already largely protected by public ownership or development planning agreements.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp2006","usgsCitation":"Oakes, E.L., Field, S.J., and Seeger, L.P., 1973, The Pine-Popple River basin — Hydrology of a wild river area, northeastern Wisconsin: U.S. Geological Survey Water Supply Paper 2006, Report: iv, 57 p.; 2 Plates: 33.50 x 29.50 inches and 31.50 x 31.00 inches, https://doi.org/10.3133/wsp2006.","productDescription":"Report: iv, 57 p.; 2 Plates: 33.50 x 29.50 inches and 31.50 x 31.00 inches","numberOfPages":"64","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":28408,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2006/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28407,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2006/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28406,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2006/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139063,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2006/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Florence County, Forest County, Marinette County","otherGeospatial":"Pine River, Popple River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.92951965332031,\n 45.874234183868346\n ],\n [\n -88.92951965332031,\n 46.08418564215268\n ],\n [\n -88.626708984375,\n 46.08418564215268\n ],\n [\n -88.626708984375,\n 45.874234183868346\n ],\n [\n -88.92951965332031,\n 45.874234183868346\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac7e4b07f02db67ae0d","contributors":{"authors":[{"text":"Oakes, Edward L.","contributorId":79517,"corporation":false,"usgs":true,"family":"Oakes","given":"Edward","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":145152,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Field, Stephen J.","contributorId":53800,"corporation":false,"usgs":true,"family":"Field","given":"Stephen","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145151,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Seeger, Lawrence P.","contributorId":17090,"corporation":false,"usgs":true,"family":"Seeger","given":"Lawrence","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":145150,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":3001,"text":"wsp2029A - 1973 - Hydrogeology of glacial drift, Mesabi Iron Range, northeastern Minnesota","interactions":[],"lastModifiedDate":"2018-04-02T12:05:48","indexId":"wsp2029A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"2029","chapter":"A","title":"Hydrogeology of glacial drift, Mesabi Iron Range, northeastern Minnesota","docAbstract":"Stratified fluvial sediments occur within the glacial drift at many places in the Mesabi Iron Range area. These sediments, which are important aquifers, occur extensively between the three main till units. The thickest and most extensive aquifer consists of glaciofluvial sediments that lie between the surficial till and the middle till unit, the bouldery till. Thickness of the glaciofluvial sediments at this stratigraphic interval is greater than 50 feet in much of the area, and transmissivity is greater than 100,000 gallons per day per foot in some places.
\nGlaciofluvial sediments underlying the bouldery till occur largely in the western half of the area. These sediments are generally less than 50 feet thick, and transmissivity is generally less than 50,000 gallons per day per foot.
\nSurficial glaciofluvial sediments are a source of ground water for high-yield wells only in the eastern part of the area in the vicinity of the Biwabik bedrock valley. Thickness of these sediments is greater than 100 feet in some places, but transmissivity is generally less than 50,000 gallons per day per foot.
\nPractical sustained yield of aquifers in glacial drift is estimated to be as much as 40 million gallons per day from known aquifers. Assuming that the ratio of area underlain by aquifer to total area is constant for the study area (about 20 percent where mapped in detail), as much as 80 million gallons per day could be developed from glacial-drift aquifers.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp2029A","collaboration":"Prepared in cooperation with the Minnesota Department of Iron Range Resources and Rehabilitation","usgsCitation":"Winter, T.C., 1973, Hydrogeology of glacial drift, Mesabi Iron Range, northeastern Minnesota: U.S. Geological Survey Water Supply Paper 2029, Document: iv, 23 p.; 3 Plates: 28.00 x 28.17 inches or smaller, https://doi.org/10.3133/wsp2029A.","productDescription":"Document: iv, 23 p.; 3 Plates: 28.00 x 28.17 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":29794,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2029a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139403,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2029a/report-thumb.jpg"},{"id":29791,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2029a/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29792,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2029a/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29793,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2029a/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","otherGeospatial":"Mesabi Iron Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -93.8,\n 47.625\n ],\n [\n -93.8,\n 47\n ],\n [\n -91.75,\n 47\n ],\n [\n -91.75,\n 47.625\n ],\n [\n -93.8,\n 47.625\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a49e4b07f02db624639","contributors":{"authors":[{"text":"Winter, Thomas C.","contributorId":84736,"corporation":false,"usgs":true,"family":"Winter","given":"Thomas","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":146127,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":26192,"text":"wri7340 - 1973 - Base of fresh ground water approximately 3,000 micromhos in the Sacramento Valley and Sacramento-San Joaquin Delta, California","interactions":[],"lastModifiedDate":"2018-12-06T14:23:22","indexId":"wri7340","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"73-40","title":"Base of fresh ground water approximately 3,000 micromhos in the Sacramento Valley and Sacramento-San Joaquin Delta, California","docAbstract":"The study area consists of about 6,600 square miles; about 5,500 square miles of the floor of the Sacramento Valley, and about 1,100 square miles of the Sacramento-San Joaquin Delta. The Sacramento Valley, as defined by Bryan (1923, p. 8), extends from Red Bluff 145 miles southward to Suisun Bay. It is bounded on the east by the Sierra Nevada, on the northeast by the Cascade Range, on the northwest by the Klamath Mountains, and the west by the Coast Ranges. Southward the valley merges with the Delta and the San Joaquin Valley. The width of the Sacramento Valley varies from about 30 miles near Red Bluff to about 60 miles on the south, and averages about 40 miles. The southern boundary of the study area coincides with the northern boundary used in an earlier study be Page (1971, 1973a).
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri7340","usgsCitation":"Berkstresser, C.F., 1973, Base of fresh ground water approximately 3,000 micromhos in the Sacramento Valley and Sacramento-San Joaquin Delta, California: U.S. Geological Survey Water-Resources Investigations Report 73-40, 22.51 x 33.21 inches, https://doi.org/10.3133/wri7340.","productDescription":"22.51 x 33.21 inches","costCenters":[],"links":[{"id":157918,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1973/0040/report-thumb.jpg"},{"id":359986,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1973/0040/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"California","otherGeospatial":"Sacramento Valley, San Joaquin Delta","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.7008056640625,\n 37.75334401310656\n ],\n [\n -120.838623046875,\n 37.75334401310656\n ],\n [\n -120.838623046875,\n 40.734770989672406\n ],\n [\n -122.7008056640625,\n 40.734770989672406\n ],\n [\n -122.7008056640625,\n 37.75334401310656\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db6489a3","contributors":{"authors":[{"text":"Berkstresser, Charles F. Jr.","contributorId":43390,"corporation":false,"usgs":true,"family":"Berkstresser","given":"Charles","suffix":"Jr.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":195963,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":41509,"text":"ofr73298 - 1973 - Aeromagnetic map of southeastern part of Lund and eastern half of Caliente 1° by 2° quadrangles, Nevada","interactions":[],"lastModifiedDate":"2021-11-30T21:13:45.797934","indexId":"ofr73298","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-298","title":"Aeromagnetic map of southeastern part of Lund and eastern half of Caliente 1° by 2° quadrangles, Nevada","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr73298","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1973, Aeromagnetic map of southeastern part of Lund and eastern half of Caliente 1° by 2° quadrangles, Nevada: U.S. Geological Survey Open-File Report 73-298, 1 Plate: 30.75 × 34.89 inches, https://doi.org/10.3133/ofr73298.","productDescription":"1 Plate: 30.75 × 34.89 inches","costCenters":[],"links":[{"id":170908,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":392270,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8807.htm"},{"id":79233,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0298/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"250000","country":"United States","state":"Nevada","otherGeospatial":"Lund and Caliente 1° by 2° quadrangles","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -115,\n 37\n ],\n [\n -114.042,\n 37\n ],\n [\n -114.042,\n 38.257\n ],\n [\n -115,\n 38.257\n ],\n [\n -115,\n 37\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db697376","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":530438,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12504,"text":"ofr7314 - 1973 - Stability of salt in the Permian salt basin of Kansas, Oklahoma, Texas, and New Mexico, with a section on dissolved salts in surface water","interactions":[],"lastModifiedDate":"2021-12-21T21:39:15.141788","indexId":"ofr7314","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-14","title":"Stability of salt in the Permian salt basin of Kansas, Oklahoma, Texas, and New Mexico, with a section on dissolved salts in surface water","docAbstract":"The Permian salt basin in the Western Interior of the United States is defined as that region comprising a series of sedimentary basins in which halite and associated salts accumulated during Permian time. The region includes the western parts of Kansas, Oklahoma, and Texas, and eastern parts of Colorado and New Mexico. \r\n\r\nFollowing a long period of general tectonic stability throughout the region during most of early Paleozoic time, there was much tectonic activity in the area of the Permian salt basin during Late Pennsylvanian and Early Permian time just before bedded salt was deposited. The Early Permian tectonism was followed by stabilization of the basins in which the salt was deposited. These salt basins were neither contemporaneous nor continuous throughout the region, so that many salt beds are also discontinuous. In general, beds in the northern part of the basin (Kansas and northern Oklahoma) are older and the salt is progressively younger towards the south. \r\n\r\nSince Permian time the Permian salt basin has been relatively stable tectonically. Regionally, the area of the salt basin has been tilted and warped, has undergone periods of erosion, and has been subject to a major incursion of the sea; but deep-seated faults or igneous intrusions that postdate Permian salt are rare. In areas of the salt basin where salt is near the surface, such as southeastern New Mexico and central Kansas, there are no indications of younger deep-seated faulting and only a few isolated igneous intrusives of post-Permian age. \r\n\r\nOn the other hand, subsidence or collapse of the land surface resulting from dissolution has been commonplace in the Permian salt basin. Some dissolution of salt deposits has probably been taking place ever since deposition of the salt more than 230 million years ago. Nevertheless, the subsurface dissolution fronts of the thick bedded-salt deposits of the Permian basin have retreated at a very slow average rate during that 230 million years.\r\n\r\nThe preservation of bedded salt from subsurface dissolution depends chiefly on the isolation of the salt from moving ground water that is not completely saturated with salt. Karst topography is a major criterion for recognizing areas where subsurface dissolution has been active in the past; therefore, the age of the karst development is needed to provide the most accurate estimate of the dissolution rate. The Ogallala Formation-of Pliocene age is probably the most widespread deposit in the Permian salt basin that can be used as a point of reference for dating the development of recent topography. It is estimated that salt has been dissolved laterally in the vicinity of Carlsbad, New Mexico, at an average rate of about 6-8 miles per million years. \r\n\r\nEstimates of future rates of salt dissolution and the resulting lateral retreat of the underground dissolution front can be projected with reasonable confidence for southeastern New Mexico on the assumption that the climatic changes there in the past 4 million years are representative of climatic changes that may be expected in the near future of geologic time. \r\n\r\nLarge amounts of salt are carried by present-day rivers in the Permian salt basin; some of the salt is derived from subsurface salt beds, but dissolution is relatively slow. Ground-water movement through the Permian salt basin is also relatively slow.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr7314","usgsCitation":"Bachman, G.O., and Johnson, R.B., 1973, Stability of salt in the Permian salt basin of Kansas, Oklahoma, Texas, and New Mexico, with a section on dissolved salts in surface water: U.S. Geological Survey Open-File Report 73-14, Report; iv, 62 p.; 1 Plate: 17.33 × 21.93 inches, https://doi.org/10.3133/ofr7314.","productDescription":"Report; iv, 62 p.; 1 Plate: 17.33 × 21.93 inches","costCenters":[],"links":[{"id":40751,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0014/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":40750,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0014/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":145222,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0014/report-thumb.jpg"},{"id":393262,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8760.htm"}],"country":"United States","state":"Kansas, New Mexico, Oklahoma, Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106,\n 30.592\n ],\n [\n -96,\n 30.592\n ],\n [\n -96,\n 40\n ],\n [\n -106,\n 40\n ],\n [\n -106,\n 30.592\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa63d","contributors":{"authors":[{"text":"Bachman, George Odell","contributorId":64249,"corporation":false,"usgs":true,"family":"Bachman","given":"George","email":"","middleInitial":"Odell","affiliations":[],"preferred":false,"id":166240,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, Ross Byron","contributorId":37339,"corporation":false,"usgs":true,"family":"Johnson","given":"Ross","email":"","middleInitial":"Byron","affiliations":[],"preferred":false,"id":166239,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3457,"text":"cir673 - 1973 - Lithium in surficial materials of the conterminous United States and partial data on cadmium","interactions":[],"lastModifiedDate":"2017-06-18T21:59:48","indexId":"cir673","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"673","title":"Lithium in surficial materials of the conterminous United States and partial data on cadmium","docAbstract":"Concentrations of lithium in 912 samples of soils and other regoliths from sites approximately 50 miles apart throughout the United States are represented on a map by symbols showing five ranges of values. A histogram of the lithium concentrations is also given. The geometric mean lithium concentration is 20.4 ppm (parts per million) for all samples, 17.3 ppm for samples from the Eastern United States, and 23.3 ppm for samples from the Western United States. Cadmium concentrations were less than 1 ppm in all but 11 of the 912 samples. Ten of these 11 samples contained from 1 to 1.5 ppm cadmium; one sample contained 10 ppm cadmium.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir673","usgsCitation":"Shacklette, H.T., Boerngen, J., Cahill, J., and Rahill, R., 1973, Lithium in surficial materials of the conterminous United States and partial data on cadmium: U.S. Geological Survey Circular 673, iii, 8 p. :illus. ;26 cm., https://doi.org/10.3133/cir673.","productDescription":"iii, 8 p. :illus. ;26 cm.","costCenters":[],"links":[{"id":30469,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1973/0673/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":118103,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1973/0673/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b13e4b07f02db6a3768","contributors":{"authors":[{"text":"Shacklette, Hansford T.","contributorId":43339,"corporation":false,"usgs":true,"family":"Shacklette","given":"Hansford","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":146959,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Boerngen, J.G.","contributorId":28974,"corporation":false,"usgs":true,"family":"Boerngen","given":"J.G.","affiliations":[],"preferred":false,"id":146958,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cahill, J.P.","contributorId":75805,"corporation":false,"usgs":true,"family":"Cahill","given":"J.P.","email":"","affiliations":[],"preferred":false,"id":146960,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Rahill, R.L.","contributorId":79752,"corporation":false,"usgs":true,"family":"Rahill","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":146961,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":30544,"text":"wri7335 - 1973 - Reconnaissance of water quality in the vicinity of Sunniland Oil Field, Collier County, Florida, 1971-72","interactions":[],"lastModifiedDate":"2018-11-02T12:47:50","indexId":"wri7335","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"73-35","title":"Reconnaissance of water quality in the vicinity of Sunniland Oil Field, Collier County, Florida, 1971-72","docAbstract":"Oil exploration in Florida began around the turn of the century in Escambia County (Gunter, 1949). Many test wells were drilled from 1900 until Humble Oil and Refining Company developed Florida's first producing well (Gulf Coast Realties Corp. No. 1) in September 1943 at Sunniland. (See fig. 1.) The first production well was drilled to 11,626 feet below sea level and had an initial production of 97 barrels of oil per day. Since this first well was developed many more have been drilled in the Sunniland field, and at this time (1973) 17 wells are producing about 50,000 barrels of oil per month (W. R. Oglesby, written commun., 1972). The Sunniland field, in north central Collier County, remained the chief oil producing field in Florida until 1966 when the Sunoco-Felda field, about 20 miles north of the Sunniland field, began producing more oil (Babcock, 1970). Oil produced in both fields is transported by pipeline to Port Everglades, on the east coast.
Anticipation of oil exploration in the Big Cypress area (fig. 1) aroused concern the effects a producing field would have on the quality of surface water in the area. The Florida Department of Natural Resources requested the U.S. Geological Survey to determine whether there have been any such effects. The 29-year old Sunniland oil field was chosen for this preliminary evaluation. A second phase of the investigation was to monitor the effects of building roads, drilling operations and other exploratory activities related to development of an oil field, on the quality of surface water in the areas of proposed exploration. This report presents the results of the first phase.
","language":"English","publisher":"U. S. Geological Survey","doi":"10.3133/wri7335","usgsCitation":"Wimberly, E., 1973, Reconnaissance of water quality in the vicinity of Sunniland Oil Field, Collier County, Florida, 1971-72: U.S. Geological Survey Water-Resources Investigations Report 73-35, iii, 10 p., https://doi.org/10.3133/wri7335.","productDescription":"iii, 10 p.","costCenters":[],"links":[{"id":160721,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1973/0035/report-thumb.jpg"},{"id":359115,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1973/0035/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Florida","county":"Collier County","otherGeospatial":"Sunniland Oil Field","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -82.25,\n 25.5\n ],\n [\n -80.75,\n 25.5\n ],\n [\n -80.75,\n 26.5\n ],\n [\n -82.25,\n 26.5\n ],\n [\n -82.25,\n 25.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acee4b07f02db67f5e5","contributors":{"authors":[{"text":"Wimberly, E.T.","contributorId":50180,"corporation":false,"usgs":true,"family":"Wimberly","given":"E.T.","email":"","affiliations":[],"preferred":false,"id":203433,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":38675,"text":"pp754A - 1973 - Glacial and postglacial geologic history of Isle Royale National Park, Michigan","interactions":[],"lastModifiedDate":"2016-12-29T10:28:25","indexId":"pp754A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"754","chapter":"A","title":"Glacial and postglacial geologic history of Isle Royale National Park, Michigan","docAbstract":"Isle Royale was overridden by glacial ice during each of the four major glaciations of the Pleistocene Epoch, and each successive glaciation essentially obliterated all direct evidence of preceding glaciations on the island. In the waning phase of the last major glaciation, the Wisconsin Glaciation, the frontal ice margin retreated northward from at least the greater part of the Lake Superior basin, then readvanced into the basin during Valders time, about 11,000 years ago. We can attribute to the Valders ice the final aspect of glaciation on Isle Royale, including both erosional and depositional features.\r\n\r\nIt is impossible to estimate the quantity of glacial debris or other surficial materials that might have been present on Isle Royale prior to the Valders readvance, but the readvancing ice appears to have removed most of what might have been present, as judged by the thin surficial cover on the eastern two-thirds of the island today. During the Valders retreat, a series of lakes formed in the Lake Superior basin in front of the retreating ice margin.\r\n\r\nThe retreating ice opened successively lower outlets, and thus the general trend of lake elevations is downward. Distinct lake stages reflect periods of relative stability during which well- defined shoreline features developed. The ice front forming the north margin of the earlier lakes probably remained south of Isle Royale until about the time of glacial Lake Beaver Bay, when it retreated to a position straddling Isle Royale west of Lake Desor. Abundant deposits of glacial debris were left upon the newly deglaciated west end of the island, and the ice front remained stable long enough to build a complex of ice-margin deposits across the island. Shorelines formed by the glacial lake associated with this ice front are found on the western part of the island about 200 feet above present Lake Superior.\r\n\r\nSubsequent renewed and complete retreat of the ice margin from Isle Royale was rapid enough that only a minor amount of glacial debris was deposited on the central and eastern parts of the island. When the ice margin reached the north edge of the Lake Superior basin, Lake Minong was formed, and the entire basin was filled for the first time since the Valders advance. Lake Minong marked a relatively stable episode in the history of the basin, and its beaches are among the best developed of the abandoned shoreline features on Isle Royale. Lake Minong beaches and later lower beaches are best developed on the southwest end of Isle Royale, where abundant glacial debris provided easily worked materials for beach construction.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"GEOLOGY OF ISLE ROYALE NATIONAL PARK, MICHIGAN","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp754A","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Huber, N.K., 1973, Glacial and postglacial geologic history of Isle Royale National Park, Michigan: U.S. Geological Survey Professional Paper 754, Report: iii, 15 p.; Plate: 30.0 x 21.5 inches, https://doi.org/10.3133/pp754A.","productDescription":"Report: iii, 15 p.; Plate: 30.0 x 21.5 inches","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true},{"id":595,"text":"U.S. Geological 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King","contributorId":51284,"corporation":false,"usgs":true,"family":"Huber","given":"N.","email":"","middleInitial":"King","affiliations":[],"preferred":false,"id":220265,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2858,"text":"wsp1969 - 1973 - Water-supply development and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T11:55:59","indexId":"wsp1969","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"1969","title":"Water-supply development and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan","docAbstract":"The Tri-County region, consisting of Clinton, Eaton, and Ingham Counties, is an area of 1,697 square miles in Michigan's Lower Peninsula and has as its hub the Lansing metropolitan area. The land surface ranges in altitude from about 700 to about 1,000 feet. The region receives an average of about 31 inches of precipitation each year.
The population is nearing 400,000 and by 1990 will be near 600,000. Average daily water use is slightly more than 30 million gallons today; by 1980 it will be about 50 million gallons, and by 1990 it will probably be about 70 million gallons.
The Tri-County region is drained by seven river systems. The median annual 7 -day mean low flows of the principal streams in these systems were measured at the point farthest downstream within the region. These values, in cubic feet per second, are as follows: Grand River, 180; Maple River, 34; Looking Glass River, 28; Red Cedar River, 30; Portage Creek, 15; Battle Creek, 20; and Thornapple River, 24-a total of 331 cubic feet per second or about 220 million gallons per day. The areal variance in 7-day low-flow runoff ranges from 0 to 0.15 cubic foot per second per square mile.
The principal source of ground water in the Tri-County region is a complex aquifer system composed of the Saginaw and Grand River Formations and some of the overlying glacial sediments. This aquifer yields between 300 and 700 gallons per minute to individual wells in much of the western half of Ingham County, in the eastern half of Clinton County, in a small area in southeastern Clinton County, and in northeastern Eaton County. In some parts of the region, the glacial sediments are favorable for development of moderate to large supplies of water. Minor aquifers in the region are the Bayport, Michigan, and Marshall Formations.
Providing water supplies in the future requires complete and comprehensive water-management programs. Such management programs involve determining which of several alternative water-development systems is the best. Some of the chief factors and methods that must be considered when planning these systems are combined use of ground and surface water, artificial recharge, treatment of wastes, use of storage reservoirs, and importation of water from the Great Lakes.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1969","usgsCitation":"Vanlier, K.E., Wood, W., and Brunett, J.O., 1973, Water-supply development and management alternatives for Clinton, Eaton, and Ingham Counties, Michigan: U.S. Geological Survey Water Supply Paper 1969, Document: vii, 111 p.; 3 Plates: 35.70 x 31.97 inches or smaller, https://doi.org/10.3133/wsp1969.","productDescription":"Document: vii, 111 p.; 3 Plates: 35.70 x 31.97 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":139081,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1969/report-thumb.jpg"},{"id":247253,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1969/plate-1.pdf","size":"5337","linkFileType":{"id":1,"text":"pdf"}},{"id":247254,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1969/plate-2.pdf","size":"10148","linkFileType":{"id":1,"text":"pdf"}},{"id":247255,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1969/plate-3.pdf","size":"13282","linkFileType":{"id":1,"text":"pdf"}},{"id":29452,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1969/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","county":"Clinton County, Eaton County, Ingham County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-84.3681,43.1172],[-84.3675,42.9561],[-84.3679,42.9439],[-84.3666,42.861],[-84.3668,42.8561],[-84.3649,42.7746],[-84.1593,42.7779],[-84.1519,42.685],[-84.146,42.5999],[-84.1402,42.4239],[-84.2539,42.4236],[-84.2607,42.4242],[-84.3676,42.4242],[-84.3677,42.4224],[-84.4864,42.4215],[-84.6026,42.4215],[-84.7207,42.4209],[-84.83,42.421],[-84.8375,42.4215],[-84.9561,42.4221],[-85.0667,42.4215],[-85.0736,42.4211],[-85.0738,42.5956],[-85.0745,42.7707],[-84.9577,42.7712],[-84.8391,42.7706],[-84.8376,42.857],[-84.8393,42.9434],[-84.8382,43.1199],[-84.6022,43.1185],[-84.3681,43.1172]]]},\"properties\":{\"name\":\"Clinton\",\"state\":\"MI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f99fe","contributors":{"authors":[{"text":"Vanlier, Kenneth Eugene","contributorId":6840,"corporation":false,"usgs":true,"family":"Vanlier","given":"Kenneth","email":"","middleInitial":"Eugene","affiliations":[],"preferred":false,"id":145915,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wood, Warren W.","contributorId":47770,"corporation":false,"usgs":false,"family":"Wood","given":"Warren W.","affiliations":[{"id":6601,"text":"Michigan State University","active":true,"usgs":false}],"preferred":false,"id":145916,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brunett, Jilann O.","contributorId":92230,"corporation":false,"usgs":true,"family":"Brunett","given":"Jilann","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":145917,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":42315,"text":"ofr73140 - 1973 - Basic data on the ultramafic rocks of the Eagle quadrangle, east-central Alaska","interactions":[],"lastModifiedDate":"2022-08-01T19:45:53.176836","indexId":"ofr73140","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-140","title":"Basic data on the ultramafic rocks of the Eagle quadrangle, east-central Alaska","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr73140","usgsCitation":"Keith, T., and Foster, H., 1973, Basic data on the ultramafic rocks of the Eagle quadrangle, east-central Alaska: U.S. Geological Survey Open-File Report 73-140, Report: 4 p.; 4 Plates: 22.18 × 35.86 inches or smaller, https://doi.org/10.3133/ofr73140.","productDescription":"Report: 4 p.; 4 Plates: 22.18 × 35.86 inches or smaller","costCenters":[],"links":[{"id":80082,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0140/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":80081,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0140/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":80080,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0140/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":80079,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0140/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":80078,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0140/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":136459,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0140/report-thumb.jpg"},{"id":106546,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8758.htm","linkFileType":{"id":5,"text":"html"},"description":"8758"}],"country":"United States","state":"Alaska","otherGeospatial":"Eagle quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -144,\n 64\n ],\n [\n -141,\n 64\n ],\n [\n -141,\n 65\n ],\n [\n -144,\n 65\n ],\n [\n -144,\n 64\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6fe4b07f02db640c1b","contributors":{"authors":[{"text":"Keith, T. E.","contributorId":33693,"corporation":false,"usgs":true,"family":"Keith","given":"T. E.","affiliations":[],"preferred":false,"id":226278,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Foster, H.L.","contributorId":34894,"corporation":false,"usgs":true,"family":"Foster","given":"H.L.","email":"","affiliations":[],"preferred":false,"id":226279,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28990,"text":"wri736 - 1973 - Geology and quality of water in the Modesto-Merced area, San Joaquin Valley, California, with a brief section on hydrology","interactions":[],"lastModifiedDate":"2019-09-05T12:53:57","indexId":"wri736","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"73-6","title":"Geology and quality of water in the Modesto-Merced area, San Joaquin Valley, California, with a brief section on hydrology","docAbstract":"The Modesto-Merced area includes about 1,800 square miles on the northeast side of the San Joaquin Valley. The physiographic units in the area are (1) Sierra Nevada, (2) dissected uplands, (3) low alluvial plains and fans, (4) river flood plains and channels, and (5) overflow lands.
Geologic units consist of consolidated rocks and unconsolidated deposits. The dominant structure of the geologic units is that of a homocline, which reflects the southwestward-tilted fault block of the Sierra Nevada. The consolidated rocks include: (1) basement complex (pre-Tertiary), (2) marine sandstone and shale (Cretaceous), (3) Ione Formation and other sedimentary rocks (Eocene), (4) Valley Springs Formation (late? Miocene), and (5) the Mehrten Formation (Miocene and Pliocene). In the eastern part of the area, the consolidated rocks generally yield small quantities of water to wells except for the Mehrten Formation which is an important aquifer.
The unconsolidated deposits include: (1) continental deposits (Pliocene and Pleistocene?), (2) lacustrine and marsh deposits (Pleistocene), (3) older alluvium (Pleistocene and Holocene?), (4) younger alluvium (Holocene), and (5) flood-basin deposits (Holocene). The continental deposits and older alluvium are the main water-yielding units in the unconsolidated deposits. The lacustrine and marsh deposits (E-clay) and the flood-basin deposits yield little water to wells, and the younger alluvium in most places probably yields only moderate quantities of water to wells.
There are three ground-water bodies in the Modesto-Merced area: (1) the unconfined water body, (2) the confined water body, and (3) the water body in consolidated rocks. The unconfined water body occurs in the unconsolidated deposits above and east of the E-clay, except in the western and southern parts of the area where clay lenses occur and semiconfined conditions exist. The confined water body occurs in the unconsolidated deposits below the E-clay and extends downward to the base of fresh water. The water body in consolidated rocks occurs under both perched and confined conditions.
Ground-water movement in the unconfined and the confined water bodies is generally westward toward the valley trough. In the unconfined water body, the water also moves toward the major rivers, and toward pumping depressions at Modesto and near El Nido. Because of the higher head in the unconfined water body, water slowly moves from it through the E-clay to the underlying confined water body.
Surface water is used extensively for irrigation in most of the study area; consequently, shallow water in the unconfined water body has to be controlled by pumping. Nevertheless, water levels near Modesto declined about 6 feet between 1958 and 1962, for the most part during the dry years 1959-61. Near El Nido, water levels declined about 70 feet between 1942 and 1967. In the confined water body, water levels were high in the winter and spring and low in the summer and fall, reflecting irrigation practices. In the southwestern part of the area, water levels in the confined water body declined about 14 feet from 1962 to 1968 and rose slightly after 1968, whereas in the northwestern part water levels remained fairly constant.
Water from the upper reaches of the Stanislaus, Tuolumne, Merced, and Chowchilla Rivers is calcium bicarbonate in chemical type and is of excellent quality. As those rivers cross the valley floor, their water quality is generally degraded by return flows from irrigated land, and in the Tuolumne River by saline water discharged from abandoned gas wells. Average dissolvedsolids content in the major rivers, as indicated by chemical analyses, do not exceed 400 mg/1 (milligrams per liter) except in the San Joaquin River where average dissolved-solids content has not exceeded 1,050 mg/l.
Water from minor streams in the area is bicarbonate in chemical type with dissolved-solids content ranging from 56 mg/1 to about 350 mg/l.
Although chloride-type fresh ground water occurs in the unconfined and confined water bodies and in the water body in consolidated rocks, most of the fresh ground water is a bicarbonate type that has a dissolved-solids content of less than 500 mg/l.
Water having dissolved solids in excess of about 2,000 mg/1 is considered to be saline. Saline water extends below the base of fresh water to the basement complex and, except in the extreme eastern part, underlies most of the study area. Saline water also occurs as lenses above the base of fresh water in the unconfined and confined water bodies.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri736","collaboration":"Prepared in cooperation with the California Department of Water Resources","usgsCitation":"Page, R.W., and Balding, G.O., 1973, Geology and quality of water in the Modesto-Merced area, San Joaquin Valley, California, with a brief section on hydrology: U.S. Geological Survey Water-Resources Investigations Report 73-6, v, 85 p., https://doi.org/10.3133/wri736.","productDescription":"v, 85 p.","costCenters":[],"links":[{"id":367180,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1973/0006/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":158886,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1973/0006/report-thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"San Joaquin Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.5,\n 37\n ],\n [\n -120,\n 37\n ],\n [\n -120,\n 38\n ],\n [\n -121.5,\n 38\n ],\n [\n -121.5,\n 37\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6842bf","contributors":{"authors":[{"text":"Page, R. W.","contributorId":17215,"corporation":false,"usgs":true,"family":"Page","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":200746,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Balding, Gary O.","contributorId":25210,"corporation":false,"usgs":true,"family":"Balding","given":"Gary","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":200747,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28913,"text":"wri7317 - 1973 - Availability of water from limestone and dolomite aquifers in southwest Ohio and the relation of water quality to the regional flow system","interactions":[],"lastModifiedDate":"2016-11-07T10:24:55","indexId":"wri7317","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"73-17","title":"Availability of water from limestone and dolomite aquifers in southwest Ohio and the relation of water quality to the regional flow system","docAbstract":"The largest ground-water supplies from the 150 to 450-foot thick carbonate-rock aquifer in southwest Ohio are available in a 2,800 squaremile area on the crest and eastern flank of the Cincinnati arch. Well production in the high-yield area is mainly from the Newburg zone, a permeable stratum in the lower part of the Bass Island group. A ' structure contour map on the top of the Lockport Dolomite shows that the Newburg zone conforms to the configuration of the Cincinnati arch. The chemical quality of the water in the consolidated-rock aquifers is intimately related to the regional flow system, and undergoes a progressive change from a calcium bicarbonate-type in recharge areas to a calcium sulfate-type in areas of natural discharge.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Columbus, OH","doi":"10.3133/wri7317","usgsCitation":"Norris, S.E., and Fidler, R.E., 1973, Availability of water from limestone and dolomite aquifers in southwest Ohio and the relation of water quality to the regional flow system: U.S. Geological Survey Water-Resources Investigations Report 73-17, iv, 42 p., https://doi.org/10.3133/wri7317.","productDescription":"iv, 42 p.","numberOfPages":"49","costCenters":[{"id":513,"text":"Ohio Water Science Center","active":true,"usgs":true}],"links":[{"id":159123,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":330803,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1973/0017/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Ohio","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -84.8089599609375,\n 40.730608477796636\n ],\n [\n -82.8094482421875,\n 40.70979201243495\n ],\n [\n -82.7215576171875,\n 38.556757147352215\n ],\n [\n -82.8424072265625,\n 38.58252615935333\n ],\n [\n -82.869873046875,\n 38.67264490154078\n ],\n [\n -82.869873046875,\n 38.7283759182398\n ],\n [\n -82.9083251953125,\n 38.758366935612784\n ],\n [\n -82.99072265625,\n 38.732661120482334\n ],\n [\n -83.0731201171875,\n 38.69408504756833\n ],\n [\n -83.133544921875,\n 38.646908247760706\n ],\n [\n -83.199462890625,\n 38.61687046392973\n ],\n [\n -83.29833984375,\n 38.59540719940386\n ],\n [\n -83.34228515625,\n 38.634036452919226\n ],\n [\n -83.4576416015625,\n 38.66406704456943\n ],\n [\n -83.5784912109375,\n 38.69408504756833\n ],\n [\n -83.638916015625,\n 38.655488159953\n ],\n [\n -83.64990234375,\n 38.62974534092597\n ],\n [\n -83.7322998046875,\n 38.64261790634527\n ],\n [\n -83.7762451171875,\n 38.655488159953\n ],\n [\n -83.84765625,\n 38.71551876930462\n ],\n [\n -83.935546875,\n 38.77549900381297\n ],\n [\n -84.0728759765625,\n 38.77121637244273\n ],\n [\n -84.1552734375,\n 38.788345355085625\n ],\n [\n -84.2156982421875,\n 38.80975079723835\n ],\n [\n -84.2376708984375,\n 38.86109762182888\n ],\n [\n -84.2706298828125,\n 38.94232097947902\n ],\n [\n -84.320068359375,\n 39.01491572891582\n ],\n [\n -84.39147949218749,\n 39.04051963289309\n ],\n [\n -84.473876953125,\n 39.027718840211605\n ],\n [\n -84.605712890625,\n 39.036252959636606\n ],\n [\n -84.6441650390625,\n 39.0831721934762\n ],\n [\n -84.70184326171875,\n 39.115144700901475\n ],\n [\n -84.72930908203125,\n 39.142842478062505\n ],\n [\n -84.7650146484375,\n 39.144972625112224\n ],\n [\n -84.7869873046875,\n 39.11727568585598\n ],\n [\n -84.81994628906249,\n 39.11088253765179\n ],\n [\n -84.8089599609375,\n 40.730608477796636\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d626","contributors":{"authors":[{"text":"Norris, Stanley Eugene","contributorId":24772,"corporation":false,"usgs":true,"family":"Norris","given":"Stanley","email":"","middleInitial":"Eugene","affiliations":[],"preferred":false,"id":200609,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fidler, Richard E.","contributorId":86313,"corporation":false,"usgs":true,"family":"Fidler","given":"Richard","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":200610,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28867,"text":"wri7339 - 1973 - Sediment transport by streams in the Upper Columbia River Basin, Washington, May 1969-June 1971","interactions":[],"lastModifiedDate":"2020-08-08T00:27:48.097803","indexId":"wri7339","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"73-39","title":"Sediment transport by streams in the Upper Columbia River Basin, Washington, May 1969-June 1971","docAbstract":"This report presents the results of a reconnaissance evaluation of the fluvial-sediment transport by streams in the 28,000-square-mile upper Columbia River basin in eastern Washington. The basin ranges in altitude from about 340 to 9,000 feet, and receives annual precipitation ranging from more than 150 inches in the mountains to less than 10 inches at the lower altitudes. A good vegetative cover is sustained in the mountains by the high precipitation, whereas vegetation is sparse in the lower semiarid parts of the basin.
In the mountainous areas snowmelt runoff transports most of the sediment during April through June. In the semiarid parts of the basin, little runoff occurs during most years, and most of the sediment is transported when heavy, warm rains fall on extensive accumulations of snow. During the 1970 and 1971 water years, the measured suspended-sediment concentrations in the upper Columbia River basin ranged from less than 1 milligram per liter in many streams to more than 200,000 milligrams per liter in Providence Coulee. The estimated long-term annual suspended-sediment yields range from less than 10 tons per square mile in many basins to more than 500 tons per square mile in Providence Coulee.
Man's activities have caused only a slight increase in the magnitude of the sediment discharge to the Columbia River. Although cultivation has initiated a large increase in erosion on the Columbia Plateau, and winds there move some of the loosened or easily eroded soils to depressions and runoff channels, sediment transport by streams has not increased greatly. This is because the little surface runoff on the plateau does not transport the soils to streams and to the Columbia River.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri7339","collaboration":"Prepared by Water Resources Division, Washington District, in cooperation with State of Washington Department of Ecology","usgsCitation":"Nelson, L.M., 1973, Sediment transport by streams in the Upper Columbia River Basin, Washington, May 1969-June 1971: U.S. Geological Survey Water-Resources Investigations Report 73-39, Report: v, 69 p.; 1 Plate: 20.29 x 22.44 inches, https://doi.org/10.3133/wri7339.","productDescription":"Report: v, 69 p.; 1 Plate: 20.29 x 22.44 inches","costCenters":[],"links":[{"id":377252,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1973/0039/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":377251,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1973/0039/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":159630,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1973/0039/report-thumb.jpg"}],"country":"United States","state":"Washington","otherGeospatial":"Columbia River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.5,\n 46\n ],\n [\n -117.5,\n 46\n ],\n [\n -117.5,\n 49\n ],\n [\n -121.5,\n 49\n ],\n [\n -121.5,\n 46\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbefc","contributors":{"authors":[{"text":"Nelson, Leonard M.","contributorId":96695,"corporation":false,"usgs":true,"family":"Nelson","given":"Leonard","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":200528,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2521,"text":"wsp1865 - 1973 - Water resources and geology of Mount Rushmore National Memorial, South Dakota","interactions":[],"lastModifiedDate":"2017-10-15T12:37:31","indexId":"wsp1865","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"1865","title":"Water resources and geology of Mount Rushmore National Memorial, South Dakota","docAbstract":"Ground water suitable for public supply can be obtained from fractured metamorphic and igneous rooks at Mount Rushmore National Memorial, S. Dak.
\nThe memorial comprises three main drainage basins: Starling basin, Lafferty Gulch basin, and East Boundary basin. Ground water is most prevalent in Lafferty Gulch basin but Starling basin contributes the most surface water.
\nThe total water supply was obtained from springs until 1967 when increasing numbers of visitors required development of additional sources. As a result of this investigation, wells 3 and 4 were drilled in Lafferty Gulch basin and East Boundary basin. Well 3 is 200 feet deep in mica schist and granite. It produced 7.3 million gallons of water in 1968 and 7.7 million gallons of water in 1969, the total supply for the memorial. Well 4 is 500 feet deep, also in mica schist and granite. It is not used at the present time (1970) but will be used in the future when more water is needed. Water from both wells is potable, but the quality of water from well 3 is superior to that from well 4.
\nMica schist is the most abundant rock in the memorial. The more prominent hills and mountains, however, are in large, northerly striking granite sills, some of which are several hundred feet thick. Pegmatite sills and dikes are also numerous. The western boundary of the memorial is at the east edge of the Harney Peak Granite batholith. The dip of schistosity and bedding in schist adjacent to the batholith is about 30 ? E. but increases across the memorial to about 65 ? E. in the northeast corner.
\nAt some locations in the memorial, granite or pegmatite sills act as ground-water dams preventing the movement of ground water down gradient. A pegmatite or granite sill is probably the cause of the accumulation of water in the vicinity of well 3. The well flows when it is not being pumped.
\nThe occurrence of ground water is dependent upon the presence of joints and fractures in the schist and granite bedrock. The rocks themselves are relatively impermeable and would yield little or no water in their unaltered state.
\nMica schist that has been intruded by granite and (or) pegmatite is more fractured and yields more ground water in the memorial than mica schist alone. This condition may be due to jointing and to the greater fracturability of the intruded rocks in the vicinity of granitic intrusions.
\nGround water is also available from alluvium in major valleys such as Starling basin and the valleys of Grizzly Bear Creek and Battle Creek.
\nEvapotranspiration is the greatest use-item in the water budget. An approximation of evapotranspiration based upon an average annual precipitation of 19 inches is 1,600 acre-feet, or 80 percent of the annual precipitation.
\nSeveral locations in the memorial have potential as future, sources of ground-water supplies. The most promising areas are near spring 6 in the southeast corner and alluvium in the valleys of Battle and Grizzly Bear Creeks.
\nDeveloped and potential water resources in the memorial probably are sufficient to meet demands beyond the year 2000.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1865","usgsCitation":"Powell, J., Norton, J.J., and Adolphson, D.G., 1973, Water resources and geology of Mount Rushmore National Memorial, South Dakota: U.S. Geological Survey Water Supply Paper 1865, Report: vi, 49 p.; Plate: 34.00 x 22.00 inches, https://doi.org/10.3133/wsp1865.","productDescription":"Report: vi, 49 p.; Plate: 34.00 x 22.00 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":28723,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1865/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138810,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1865/report-thumb.jpg"},{"id":28724,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1865/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","otherGeospatial":"Mount Rushmore National Memorial","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.46400260925293,\n 43.873705074113886\n ],\n [\n -103.46400260925293,\n 43.88391319597796\n ],\n [\n -103.45061302185059,\n 43.88391319597796\n ],\n [\n -103.45061302185059,\n 43.873705074113886\n ],\n [\n -103.46400260925293,\n 43.873705074113886\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db687e04","contributors":{"authors":[{"text":"Powell, J.E.","contributorId":27030,"corporation":false,"usgs":true,"family":"Powell","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":145336,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Norton, James Jennings","contributorId":59412,"corporation":false,"usgs":true,"family":"Norton","given":"James","email":"","middleInitial":"Jennings","affiliations":[],"preferred":false,"id":145337,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Adolphson, D. G.","contributorId":106081,"corporation":false,"usgs":true,"family":"Adolphson","given":"D.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":145338,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5974,"text":"pp776 - 1973 - Stratigraphy and geologic history of the Montana group and equivalent rocks, Montana, Wyoming, and North and South Dakota","interactions":[{"subject":{"id":45944,"text":"ofr69106 - 1969 - Paleogeographic maps of the Telegraph Creek, Eagle, Claggett, Judith River, Bearpaw, and Fox Hills times of late Cretaceous Epoch in the western interior region","indexId":"ofr69106","publicationYear":"1969","noYear":false,"title":"Paleogeographic maps of the Telegraph Creek, Eagle, Claggett, Judith River, Bearpaw, and Fox Hills times of late Cretaceous Epoch in the western interior region"},"predicate":"SUPERSEDED_BY","object":{"id":5974,"text":"pp776 - 1973 - Stratigraphy and geologic history of the Montana group and equivalent rocks, Montana, Wyoming, and North and South Dakota","indexId":"pp776","publicationYear":"1973","noYear":false,"title":"Stratigraphy and geologic history of the Montana group and equivalent rocks, Montana, Wyoming, and North and South Dakota"},"id":1}],"lastModifiedDate":"2017-01-03T14:54:45","indexId":"pp776","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"776","title":"Stratigraphy and geologic history of the Montana group and equivalent rocks, Montana, Wyoming, and North and South Dakota","docAbstract":"During Late Cretaceous time a broad north-trending epicontinental sea covered much of the western interior of North America and extended from the Gulf of Mexico to the Arctic Ocean. The sea was bounded on the west by a narrow, unstable, and constantly rising cordillera which extended from Central America to Alaska and which separated the sea from Pacific oceanic waters. The east margin of the sea was bounded by the low-lying stable platform of the central part of the United States.
Rocks of the type Montana Group in Montana and equivalent rocks in adjacent States, which consist of eastward-pointing wedges of shallow-water marine and nonmarine strata that enclose westward-pointing wedges of fine-grained marine strata, were deposited in and marginal to this sea. These rocks range in age from middle Santonian to early Maestrichtian and represent a time span of about 14 million years. Twenty-nine distinctive ammonite zones, each with a time span of about half a million years, characterize the marine strata.
Persistent beds of bentonite in the transgressive part of the Claggett and Bearpaw Shales of Montana and equivalent rocks elsewhere represent periods of explosive volcanism and perhaps concurrent subsidence along the west shore in the vicinity of the Elkhorn Mountains and the Deer Creek volcanic fields in Montana. Seaward retreat of st randlines, marked by deposition of the Telegraph Creek, Eagle, Judith River, and Fox Hills Formations in Montana and the Mesaverde Formation in Wyoming, may be attributed to uplift in near-coastal areas and to an increase in volcaniclastic rocks delivered to the sea.
Rates of transgression and regression determined for the Montana Group in central Montana reveal that the strandline movement was more rapid during times of transgression. The regression of the Telegraph Creek and Eagle strandlines averaged about 50 miles per million years compared with a rate of about 95 miles per million years for the advance of the strand-line during Claggett time. The Judith River regression averaged about 60 miles per million years compared with movement of the strandline during the Bearpaw advance of about 70 miles per million years.
The final retreat of marine waters from Montana, marked by the Fox Hills regression, was about 35 miles per million years at first, but near the end of the regression it accelerated to a rate of about 500 miles per million years.
Rates of sedimentation range from less than 50 feet per million years in the eastern parts of North and South Dakota to at least 2,500 feet in western Wyoming. The low rates in the Dakotas correspond well with modern rates in the open ocean, and the rates in western Wyoming approach the rate of present coastal sedimentation.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp776","usgsCitation":"Gill, J.R., and Cobban, W.A., 1973, Stratigraphy and geologic history of the Montana group and equivalent rocks, Montana, Wyoming, and North and South Dakota: U.S. Geological Survey Professional Paper 776, iii, 37 p., https://doi.org/10.3133/pp776.","productDescription":"iii, 37 p.","numberOfPages":"36","costCenters":[],"links":[{"id":332510,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0776/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139769,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0776/report-thumb.jpg"}],"country":"United States","state":"Montana, North Dakota, South Dakota, 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\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1fe4b07f02db6aabc6","contributors":{"authors":[{"text":"Gill, James R.","contributorId":44904,"corporation":false,"usgs":true,"family":"Gill","given":"James","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":151896,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cobban, William Aubrey","contributorId":78317,"corporation":false,"usgs":true,"family":"Cobban","given":"William","email":"","middleInitial":"Aubrey","affiliations":[],"preferred":false,"id":151897,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":17968,"text":"ofr737 - 1973 - Geologic and hydrologic summary of salt domes in Gulf Coast region of Texas, Louisiana, Mississippi, and Alabama","interactions":[],"lastModifiedDate":"2025-07-31T20:27:27.244042","indexId":"ofr737","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"73-7","title":"Geologic and hydrologic summary of salt domes in Gulf Coast region of Texas, Louisiana, Mississippi, and Alabama","docAbstract":"There are 263 known or suspected onshore salt domes in the Texas-Louisiana-Mississippi-Alabama portion of the Gulf Coast geosyncline. The top of the salt in 148 of them is probably deeper than desirable for a waste repository site, and 79 of those that are shallow enough are probably unavailable for a site because of present use by industry for gas storage or production of oil, salt, or sulfur. In this report we have compiled the available geologic and hydrologic background data pertinent to the evaluation of the remaining 36 known or suspected salt domes as potential sites for waste storage. There are three parts to this compilations: 1) summaries of the geology and hydrology of the salt-dome province as a whole; 2) summaries of the physiography, climate, geology, and hydrology of each of the five salt-dome basins that occur within the province; and 3) an appendix of background data for each of the 36 potentially acceptable domes. \r\n\r\nThe distribution of salt domes in the province is genetically related to areas of relative subsidence that formed basins or depocenters within the Gulf Coast geosyncline. In some cases, as in northeast Texas and south Louisiana, the locations of individual domes or groups of domes are related to deep movement of salt along axial trends. The salt domes in the interior salt-dome subprovince are probably more structurally stable than those of the coastal subprovince because salt diapirism is inferred to have ceased around Miocene time in the interior but may still be active in parts of the coastal subprovince. Although the size and shape of many domes is unknown or can only be roughly approximated, each of the five basins in the province appears to contain potentially acceptable domes of adequate size for a repository. We recognize no pattern to the distribution of salt-dome size. Caprock thicknesses vary greatly within each salt-dome basin,and we recognize no pattern to the variations. Among the potentially acceptable domes, the depths to the top of the salt are generally greatest in the Mississippi salt-dome basin, where all tops are more than 1,500 feet deep. Intermediate depths of about 1,000 feet are common in the east Texas-south Louisiana salt-dome basin. Depths to salt tops in the north Louisiana and northeast Texas basins are variable but most are less than 1,000 feet.\r\n\r\nAvailable drilling records are generally adequate to determine the number of wells drilled on or in the vicinity of individual domes and also the well locations. The numbers of wells vary widely within each salt-dome basin. More salt domes are currently available for use as repository sites in the interior subprovince than in the coastal subprovince, where the pressure for industrial use of domes is high. In the interior subprovince many of the potentially acceptable domes are located beneath hilly well-drained terrain that is not subject to flooding or other surface-water problems. Although topographic depressions occupied by shallow lakes, swamps, or 'salines' occur over several of the domes, they are generally flanked by topographically high ground where surface facilities could be sited without complications.A few of the potentially acceptable domes are located beneath floodplains where surface facilities might face hazards from flooding. In the coastal subprovince several of the potentially acceptable domes are located in relatively flat poorly drained terrain where surface flooding might constitute a potential hazard. \r\n\r\nThe availability of fresh to slightly saline ground water varies considerably within each salt-dome basin. We have outlined some of the factors that are responsible for the variations and have provided or referred to maps and geohydrologic cross sections that illustrate the general distribution of fresh to slightly saline water. The top of the salt in about half of the known potentially acceptable domes is below the regional base of the fresh to slightly saline ground-water system, but in a few of","language":"English","publisher":"U. S. Geological Survey,","doi":"10.3133/ofr737","usgsCitation":"Anderson, R.E., Eargle, D.H., and Davis, B.O., 1973, Geologic and hydrologic summary of salt domes in Gulf Coast region of Texas, Louisiana, Mississippi, and Alabama: U.S. Geological Survey Open-File Report 73-7, Report: xiii, 294 p.; 6 Plate: 31.76 x 11.27 inches or smaller, https://doi.org/10.3133/ofr737.","productDescription":"Report: xiii, 294 p.; 6 Plate: 31.76 x 11.27 inches or smaller","costCenters":[],"links":[{"id":493285,"rank":9,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8839.htm","linkFileType":{"id":5,"text":"html"}},{"id":47212,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0007/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47211,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0007/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47207,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0007/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":151245,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1973/0007/report-thumb.jpg"},{"id":47210,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0007/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47209,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0007/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47213,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1973/0007/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47208,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1973/0007/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Alabama, Louisiana, Mississippi, Texas","otherGeospatial":"Gulf Coast region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -96.76730070250153,\n 32.17023484133644\n ],\n [\n -98.75524870217694,\n 26.91436540558027\n ],\n [\n -97.33850253200262,\n 25.769699667722122\n ],\n [\n -94.02150774872237,\n 28.829616636304948\n ],\n [\n -87.71739762029995,\n 28.891748873149012\n ],\n [\n -87.85369605864722,\n 31.719171653381665\n ],\n [\n -96.76730070250153,\n 32.17023484133644\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a818f","contributors":{"authors":[{"text":"Anderson, R. Ernest","contributorId":104484,"corporation":false,"usgs":true,"family":"Anderson","given":"R.","email":"","middleInitial":"Ernest","affiliations":[],"preferred":false,"id":178300,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Eargle, Dolan H.","contributorId":104514,"corporation":false,"usgs":true,"family":"Eargle","given":"Dolan","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":178301,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Davis, Beth O.","contributorId":63365,"corporation":false,"usgs":true,"family":"Davis","given":"Beth","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":178299,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5748,"text":"pp712B - 1973 - Geohydrology of the eastern part of Pahute Mesa, Nevada Test Site, Nye County, Nevada","interactions":[],"lastModifiedDate":"2025-04-15T20:00:20.454537","indexId":"pp712B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1973","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":"712","chapter":"B","title":"Geohydrology of the eastern part of Pahute Mesa, Nevada Test Site, Nye County, Nevada","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp712B","usgsCitation":"Blankennagel, R.K., and Weir, J.E., 1973, Geohydrology of the eastern part of Pahute Mesa, Nevada Test Site, Nye County, Nevada: U.S. Geological Survey Professional Paper 712, Report: 34 p.; 3 Plates: 35.50 x 18.51 inches, https://doi.org/10.3133/pp712B.","productDescription":"Report: 34 p.; 3 Plates: 35.50 x 18.51 inches","costCenters":[],"links":[{"id":484614,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_5011.htm","linkFileType":{"id":5,"text":"html"}},{"id":22055,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0712b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":22054,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0712b/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":22053,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0712b/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":22052,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0712b/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":140261,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0712b/report-thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Nevada Test Site, Pahute Mesa","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.625,\n 37.3833\n ],\n [\n -116.625,\n 37.125\n ],\n [\n -116.25,\n 37.125\n ],\n [\n -116.25,\n 37.3833\n ],\n [\n -116.625,\n 37.3833\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8850","contributors":{"authors":[{"text":"Blankennagel, Richard K.","contributorId":55423,"corporation":false,"usgs":true,"family":"Blankennagel","given":"Richard","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":151516,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weir, J. E. Jr.","contributorId":102476,"corporation":false,"usgs":true,"family":"Weir","given":"J.","suffix":"Jr.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":151517,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70038039,"text":"70038039 - 1973 - Hydrologic Data of the Neponset and Weymouth River Basins, Massachusetts","interactions":[],"lastModifiedDate":"2015-02-09T09:17:45","indexId":"70038039","displayToPublicDate":"1974-01-01T10:48:00","publicationYear":"1973","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":367,"text":"Massachusetts Hydrologic - Data Report","active":false,"publicationSubtype":{"id":6}},"seriesNumber":"14","title":"Hydrologic Data of the Neponset and Weymouth River Basins, Massachusetts","docAbstract":"The Neponset, Weymouth Fore, and Weymouth Back River basins occupy an area of 183 square miles in eastern Massachusetts south of Boston and Braintree, Brockton, Canton, Dedham, Dover, Foxborough, Hingham, Holbrook, Medfield, Milton, Norwood, Quincy, Randolph, Rockland, Sharon, Stoughton, Walpole, Westwood, and Weymouth.
\nHydrologic data presented in this report were collected during an investigation of the water resources in the areas of these basins that are upstream from tide effect or heavy urbanization. This investigation was conducted by the U.S. Geological Survey in cooperation with the Massachusetts Water Resources Commission. The data are released in order to make available to the public basic hydrologic and related information that will facilitate the planning of water-resources development and will complement an interpretive report, \"Hydrology and water resources of the Neoponset and Weymouth River basins, Massachusetts\" (HA-484).
\nThe well and boring data contained herein were selected from a larger group of data in order to minimize redundancy of information for intensely drilled areas. All of the data are on filed and available for inspection at the office of the U.S. Geological Survey, Water Resources Division, Boston, Massachusetts.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Boston, Massachusetts","doi":"10.3133/70038039","collaboration":"Prepared in cooperation with the Commonwealth of Massachusetts, Water Resources Commission","usgsCitation":"Brackley, R., Fleck, W.B., and Willey, R.E., 1973, Hydrologic Data of the Neponset and Weymouth River Basins, Massachusetts: Massachusetts Hydrologic - Data Report 14, Report: 51 p.; Plate: 47.12 x 35.64 inches, https://doi.org/10.3133/70038039.","productDescription":"Report: 51 p.; Plate: 47.12 x 35.64 inches","numberOfPages":"56","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":264632,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038039/plate-1.pdf","size":"16.2 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":264633,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70038039/report.pdf","size":"4.3 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":264634,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70038039/report-thumb.jpg"}],"scale":"31680","country":"United States","state":"Massachusetts","otherGeospatial":"Neponset River, Weymouth River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.29852294921875,\n 42.06968462804663\n ],\n [\n -71.29852294921875,\n 42.35245491952619\n ],\n [\n -70.8837890625,\n 42.35245491952619\n ],\n [\n -70.8837890625,\n 42.06968462804663\n ],\n [\n -71.29852294921875,\n 42.06968462804663\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a3510e4b0c8380cd5fc27","contributors":{"authors":[{"text":"Brackley, R. A.","contributorId":16851,"corporation":false,"usgs":true,"family":"Brackley","given":"R. A.","affiliations":[],"preferred":false,"id":463316,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fleck, William B.","contributorId":17587,"corporation":false,"usgs":true,"family":"Fleck","given":"William","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":463317,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Willey, Richard E.","contributorId":30972,"corporation":false,"usgs":true,"family":"Willey","given":"Richard","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463318,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70207542,"text":"70207542 - 1973 - Chemical variation related to the stratigraphy of the Columbia River basalt","interactions":[],"lastModifiedDate":"2020-06-03T15:19:39.027101","indexId":"70207542","displayToPublicDate":"1973-12-23T11:10:34","publicationYear":"1973","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":"Chemical variation related to the stratigraphy of the Columbia River basalt","docAbstract":"Study of major element chemical analyses of Columbia River basalt leads to a grouping of most of the analyses into 11 chemical types which are distinguished with little overlap on a SiO2-MgO variation diagram. Other diagnostic variation diagrams are total iron (‘FeO’)-MgO, K2O-MgO, and TiO2-MgO.
A four-unit informal stratigraphy has been adopted in order to define the relations between chemical composition and stratigraphic position. From oldest to youngest, the four stratigraphic units are (1) lower basalt of Bond (1963) and Picture Gorge basalt, (2) lower Yakima basalt, (3) middle Yakima basalt, and (4) upper Yakima basalt.
Most of the Picture Gorge and lower basalt flows are relatively rich in MgO (approximately 4.5 to 7.1 percent) and are distinguished by intermediate SiO2 relative to MgO. Furthermore, the Picture Gorge basalt generally has low K2O relative to MgO. The lower Yakima basalt consists almost entirely of flows with relatively low MgO content (approximately 3.0 to 5.5 percent) and with the highest SiO2 relative to MgO of any flows of the Columbia River basalt. The middle Yakima basalt contains flows of three distinct chemical types, which together cover the same MgO range as the lower Yakima flows but which have considerably lower SiO2 and higher ‘FeO’ and TiO2 relative to MgO. Flows in the upper Yakima basalt are of diverse composition; two of the youngest flows are distinguished by having the lowest SiO2 and highest ‘FeO’, TiO2, and P2O5 relative to MgO of any analyzed Columbia River basalt.
Flows of one or more chemical types may form the dominant lithology in a stratigraphic unit, but single flows of the same chemical types may occur in any stratigraphic unit.
Some lava sampled in the eastern part of the plateau has more TiO2 than does lava of otherwise similar composition sampled in the western part of the plateau. This is tentatively interpreted as reflecting a heterogeneous composition for the mantle beneath the Columbia Plateau.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1973)84<371:CVRTTS>2.0.CO;2","usgsCitation":"Wright, T., Grolier, M.J., and Swanson, D., 1973, Chemical variation related to the stratigraphy of the Columbia River basalt: GSA Bulletin, v. 84, no. 2, p. 371-386, https://doi.org/10.1130/0016-7606(1973)84<371:CVRTTS>2.0.CO;2.","productDescription":"16 p.","startPage":"371","endPage":"386","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":370643,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Oregon, Washington","otherGeospatial":"Columbia River Basalt","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.87255859374999,\n 47.635783590864854\n ],\n [\n -119.4873046875,\n 48.07807894349862\n ],\n [\n -120.30029296875,\n 47.724544549099676\n ],\n [\n -121.025390625,\n 47.264320080254805\n ],\n [\n -121.33300781249999,\n 46.63435070293566\n ],\n [\n -121.48681640624999,\n 45.84410779560204\n ],\n [\n -121.53076171875,\n 45.259422036351694\n ],\n [\n -118.47656249999999,\n 45.398449976304086\n ],\n [\n -117.158203125,\n 45.9511496866914\n ],\n [\n -116.19140625,\n 47.05515408550348\n ],\n [\n -116.87255859374999,\n 47.635783590864854\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"84","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Wright, Thomas L. twright@usgs.gov","contributorId":3890,"corporation":false,"usgs":true,"family":"Wright","given":"Thomas L.","email":"twright@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":778412,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Grolier, Maurice J.","contributorId":98292,"corporation":false,"usgs":true,"family":"Grolier","given":"Maurice","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":778413,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Swanson, Don 0000-0002-1680-3591 donswan@usgs.gov","orcid":"https://orcid.org/0000-0002-1680-3591","contributorId":168817,"corporation":false,"usgs":true,"family":"Swanson","given":"Don","email":"donswan@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":778414,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70241487,"text":"70241487 - 1973 - Variations in Sr, Rb, K, Na, and Initial Sr87/Sr86 in Mesozoic Granitic Rocks and Intruded Wall Rocks in Central California","interactions":[],"lastModifiedDate":"2023-03-21T19:00:05.843808","indexId":"70241487","displayToPublicDate":"1973-11-01T13:50:16","publicationYear":"1973","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Variations in Sr, Rb, K, Na, and Initial Sr87/Sr86 in Mesozoic Granitic Rocks and Intruded Wall Rocks in Central California","title":"Variations in Sr, Rb, K, Na, and Initial Sr87/Sr86 in Mesozoic Granitic Rocks and Intruded Wall Rocks in Central California","docAbstract":"Initial Sr87/Sr86 of granitic rocks which are exposed north of the Garlock fault in California, and which represent the entire 130-m.y. time span of emplacement during the Mesozoic, ranges mainly from 0.7031 to 0.7082, with one value of 0.7094. A systematic areal variation, independent of age, exists for initial Sr87/Sr86 in these granitic rocks and is the same as the areal variation in initial Sr87/Sr86 of superjacent upper Cenozoic basalts and andesites.
Two values of initial Sr87/Sr86, 0.7040 and 0.7060, mark natural separations of granitic rock data on K-Rb, K-Sr, and Rb/Sr-Rb variation diagrams, and also, when contoured, seem to represent geographic markers of paleo-geographic, geochemical, and physiographic significance. Upper Precambrian sedimentary and metamorphic rocks in California crop out only in the region where initial Sr87/Sr86 of granitic rocks is greater than 0.7060. A line of initial Sr87/Sr86 = 0.7060 is approximately coincident with the boundary between Paleozoic eugeosynclinal and miogeosynclinal rocks. Granitic rocks intruded into Paleozoic miogeosynclinal rocks have initial Sr87/Sr86 greater than 0.7060, whereas those intruded into eugeosynclinal Paleozoic rocks have initial Sr87/Sr86 less than 0.7060. The line of initial Sr87/Sr86 = 0.7040 is the eastern limit of principal exposures of ultramafic rocks, the western limit of Cretaceous granitic rocks, and is coincident with an abrupt change in “topographic expression” on the Bouguer gravity map of California. Correlation of the isotopic variations with these major crustal features suggests that there has been a sharp lateral contrast in crust-mantle chemistry across the region of study that has been fixed in position from the Precambrian to the present time.
The chemical and isotopic variations observed are best explained if the parent magmas of the majority of granitic rocks investigated were derived in a region that was laterally variable in composition and in a zone of melting that intersected both upper mantle and lower crust. However, some igneous rocks, such as Jurassic volcanic rocks in wall rocks and roof pendants and some granitic rocks with high strontium concentrations and low Rb-Sr ratios, suggest that deeper sources are also involved in the total spectrum of igneous rocks in the region.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1973)84<3489:VISRKN>2.0.CO;2","usgsCitation":"Kistler, R.W., and Peterman, Z.E., 1973, Variations in Sr, Rb, K, Na, and Initial Sr87/Sr86 in Mesozoic Granitic Rocks and Intruded Wall Rocks in Central California: Geological Society of America Bulletin, v. 84, no. 11, p. 3489-3512, https://doi.org/10.1130/0016-7606(1973)84<3489:VISRKN>2.0.CO;2.","productDescription":"23 p.","startPage":"3489","endPage":"3512","costCenters":[],"links":[{"id":414482,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -122.20533281313979,\n 40.42429466387006\n ],\n [\n -121.13423967713446,\n 38.76444227129281\n ],\n [\n -120.76097994792032,\n 38.02674663755306\n ],\n [\n -120.2822337734942,\n 37.267563216163396\n ],\n [\n -119.21925497942821,\n 36.443003503084654\n ],\n [\n -118.98393906318458,\n 35.37174364660258\n ],\n [\n -118.58633630815233,\n 34.780728225669776\n ],\n [\n -117.89661724330026,\n 35.27243450243415\n ],\n [\n -117.59638659154092,\n 35.39820547854103\n ],\n [\n -116.50906477165633,\n 35.550192445638686\n ],\n [\n -116.33054924898866,\n 36.35156375846992\n ],\n [\n -119.99823180561347,\n 39.02642088257426\n ],\n [\n -119.99823180561347,\n 40.769325113633926\n ],\n [\n -120.85835205119372,\n 41.11868651760588\n ],\n [\n -121.51561374828796,\n 41.13091124098662\n ],\n [\n -122.05116031629072,\n 40.78775861945306\n ],\n [\n -122.20533281313979,\n 40.42429466387006\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"84","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Kistler, Ronald Wayne","contributorId":27857,"corporation":false,"usgs":true,"family":"Kistler","given":"Ronald","email":"","middleInitial":"Wayne","affiliations":[],"preferred":false,"id":867000,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Peterman, Zell E. 0000-0002-5694-8082 peterman@usgs.gov","orcid":"https://orcid.org/0000-0002-5694-8082","contributorId":167699,"corporation":false,"usgs":true,"family":"Peterman","given":"Zell","email":"peterman@usgs.gov","middleInitial":"E.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":867001,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70241824,"text":"70241824 - 1973 - Nodal tidal cycle of 18.6 yr.: Its importance in sea-level curves of the east coast of the United States and its value in explaining long-term sea-level changes","interactions":[],"lastModifiedDate":"2023-03-28T15:35:45.931617","indexId":"70241824","displayToPublicDate":"1973-11-01T10:18:44","publicationYear":"1973","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1796,"text":"Geology","active":true,"publicationSubtype":{"id":10}},"title":"Nodal tidal cycle of 18.6 yr.: Its importance in sea-level curves of the east coast of the United States and its value in explaining long-term sea-level changes","docAbstract":"The 18.6-yr cycle of the Moon's nodes dominates the annual means of high water, low water, and range at Boston and at other East Coast harbors. The maxima and minima of the high-water and range curves agree closely with the 180° and 0° long. yr, respectively, of the Moon's ascending node, and are fairly well accounted for by tide-prediction equations. The curve of annual mean sea level also reflects the cycle, but more weakly. Recognition of the cyclical nature of tidal data both simplifies and clarifies assessments of longer term sea-level trends and points to the need to include only multiples of entire cycles in the computations of these trends. When the curves of mean high water and range are used, it is possible to recognize long-term sea-level trends rapidly and to determine whether these are attributable to tidal or nontidal causes. The data suggest that the secular sea-level rise during the 20th century is tidal in origin and may be caused by vertical movement of the oceanic floor. This has the effect of reducing the volume of ocean basins, and, by changing basin geometry, alters the characteristics of terrestrial tidal constituents (standing waves).
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