Basic data on water quantity, chemical quality, and suspended sediment are tabulated to record the conditions existing in two basins near Philadelphia, each about 32 square miles in area. The basins in 1970 are agricultural land for the most part, but urban and industrial development is imminent as the Philadelphia metropolitan area expands. Hopefully, as changes caused by urbanization occur in future years, data published herein will be useful as a base for comparison.
Pickering Creek basin has a higher population than the upper East Branch Brandywine Creek basin. The two are comparable in discharge characteristics and in shapes and sizes of channels, but the Pickering Creek basin is producing a considerably larger suspended-sediment load. Also the effects of urbanization are discernible in some chemical parameters.
During the study, a small subbasin, one-half square mile in area, was converted from agricultural use to an industrial park. This change resulted in a marked increase in sulfates, nitrates, chlorides, and dissolved solids in the streamflow.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp701A","usgsCitation":"Miller, R.A., Troxell, J., Leopold, L.B., Patrick, R., and Grant, R.R., 1971, Hydrology of two small river basins in Pennsylvania before urbanization, with a section on observation of stream fauna: U.S. Geological Survey Professional Paper 701, iv, 57 p., https://doi.org/10.3133/pp701A.","productDescription":"iv, 57 p.","numberOfPages":"68","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":117927,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0701a/report-thumb.jpg"},{"id":33442,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0701a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Upper East Branch Brandywine Creek, Pickering Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.89355468749999,\n 39.96870074491696\n ],\n [\n -75.45135498046875,\n 39.96870074491696\n ],\n [\n -75.45135498046875,\n 40.16418235037417\n ],\n [\n -75.89355468749999,\n 40.16418235037417\n ],\n [\n -75.89355468749999,\n 39.96870074491696\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fc7cc","contributors":{"authors":[{"text":"Miller, R. Adam","contributorId":21540,"corporation":false,"usgs":true,"family":"Miller","given":"R.","email":"","middleInitial":"Adam","affiliations":[],"preferred":false,"id":152357,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Troxell, John","contributorId":83517,"corporation":false,"usgs":true,"family":"Troxell","given":"John","email":"","affiliations":[],"preferred":false,"id":152359,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Leopold, Luna Bergere","contributorId":93884,"corporation":false,"usgs":true,"family":"Leopold","given":"Luna","email":"","middleInitial":"Bergere","affiliations":[],"preferred":false,"id":152360,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Patrick, Ruth","contributorId":95055,"corporation":false,"usgs":true,"family":"Patrick","given":"Ruth","email":"","affiliations":[],"preferred":false,"id":152361,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Grant, Robert R. Jr.","contributorId":75524,"corporation":false,"usgs":true,"family":"Grant","given":"Robert","suffix":"Jr.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":152358,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":2629,"text":"wsp1870D - 1971 - Summary of floods in the United States during 1966","interactions":[],"lastModifiedDate":"2017-09-20T16:39:50","indexId":"wsp1870D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1870","chapter":"D","title":"Summary of floods in the United States during 1966","docAbstract":"This report describes the outstanding floods in the United States during 1966. The four most destructive floods occurred during March-April in the Red River of the North basin in northwestern Minnesota, during April-May in northeastern Texas, in August, in east-central Nebraska, and in December, in the Southwestern United States. \r\n\r\nFor the second consecutive year, there was severe flooding in the Red River of the North basin in Minnesota during ,the spring snowmelt period. Unseasonally warm temperature caused rapid melting of a heavy snow cover, with water equivalent ranging from 5 to 7 inches, which covered .the northern two-thirds of the basin. Peak discharges were maximum of record at three gaging sites having periods of record ranging from 20 to 30 years, ,and peak discharges exceeded 50-year floods at nine sites. Damage from the flood was estimated at $10 million. In the period April 22-29, from 20 to 26 inches of rain fell in parts of the Sabine River basin in northeastern Texas. and high rates of runoff occurred from the headwaters of the Sulphur River southward .to the Trinity River basin. Flood damage was estimated at $12 million, and at least 25 persons lost their lives. \r\n\r\nSevere floods occurred along the Loup River ,and its tributaries in east-central Nebraska on August 12-14. The .peak discharge at nearly all gaging stations in the flood area exceeded the previous maximum of record. The floods we re caused by heavy rains of from 13 to 17 inches in about 24 hours. The storm was the most widespread in the area since 1896 and may have exceeded the area of the 1896 storm. The floods were unusual because of the consistently high discharges throughout a large flood area. Flood damage was estimated at $11 million. \r\n\r\nIn early December a storm moved eastward from the Pacific coast in southern California into Southwestern United States. Intense precipitation occurred around the mountain ranges of south-central California and in and extending from southeastern Nevada across the southwestern corner of Utah to the Grand Canyon and southward to the mountains of central Arizona. Discharges on many streams exceeded the previous maximums known, and the flood was particularly damaging because of the large area involved.\r\n\r\nIn .addition to these four floods, 19 others of lesser magnitude are considered important enough to be included in this annual summary.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey ;","doi":"10.3133/wsp1870D","isbn":"pbk","usgsCitation":"Rostvedt, J., 1971, Summary of floods in the United States during 1966: U.S. Geological Survey Water Supply Paper 1870, v, 99 p. :ill. ;24 cm., https://doi.org/10.3133/wsp1870D.","productDescription":"v, 99 p. :ill. ;24 cm.","costCenters":[{"id":5050,"text":"WY-MT Water Science Center","active":true,"usgs":true}],"links":[{"id":28946,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1870d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138163,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1870d/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db69924b","contributors":{"authors":[{"text":"Rostvedt, J.O.","contributorId":24757,"corporation":false,"usgs":true,"family":"Rostvedt","given":"J.O.","email":"","affiliations":[],"preferred":false,"id":145527,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23366,"text":"ofr72166 - 1971 - Water-level changes 1964-71, northern High Plains of Colorado","interactions":[],"lastModifiedDate":"2018-01-09T16:34:55","indexId":"ofr72166","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"72-166","title":"Water-level changes 1964-71, northern High Plains of Colorado","docAbstract":"Ground-water withdrawals for irrigation increased from about 84,000 acre-feet to 430,000 acre-feet per year between 1960 and 1970 in the northern High Plains of Colorado, causing significant water-level declines in areas where high-capacity wells are concentrated. The number of wells increased from about 500 in 1960 to 2,560 in 1970. In 1968 the U.S. Geological Survey began a study in cooperation with the Colorado Water Conservation Board; the Colorado Division of Water Resources, Office of the State Engineer; and the Management Districts of the northern High Plains to provide information for administration and management of the vital ground-water reserves of the northern High Plains.
The northern High Plains of Colorado is formed from an erosional remanent of the Ogallala Formation of Pliocene Age that extends from the South Platte River on the north to the Arkansas River on the south, and from Limon, Colo. on the west across the Colorado State line on the east (fig. 1). This area includes all or part of 11 counties and contains about 9,500 square miles. General information describing the ground-water resources of the northern High Plains of Colorado is presented in table 1. Plate 1 shows the net changes in water level between 1964 and 1971. Other published water-level change maps are for the period from 1964-68 and 1964-69 (Boettcher and others, 1969). The map (pl. 1) is based on annual water-level measurements made in 1964 and 1971 in about 300 wells tapping the Ogallala aquifer. Areas with either a net decline or a net rise are shown. Large declines recorded near Yuma and Burlington correspond to relatively high concentrations (2 per sq mi) of high-capacity wells. Also included in this report are 11 hydrographs typical of the water-level changes during this period (figs. 2-4). The hydrographs show water-level changes from 1964, or as early as 1956 to 1971, and illustrate the consistency of water-level change rates. Because proper management of ground-water resources requires systematic and valid basic data, the annual water-level measurements should continue.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr72166","issn":"0094-9140","usgsCitation":"Hofstra, W.E., Klein, J.M., and Major, T.J., 1971, Water-level changes 1964-71, northern High Plains of Colorado: U.S. Geological Survey Open-File Report 72-166, Report: i, 10 p.; Plate: 13.58 x 27.32 inches, https://doi.org/10.3133/ofr72166.","productDescription":"Report: i, 10 p.; Plate: 13.58 x 27.32 inches","numberOfPages":"14","costCenters":[],"links":[{"id":156735,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":52656,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1972/0166/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Colorado","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.85,\n 38\n ],\n [\n -102,\n 38\n ],\n [\n -102,\n 41\n ],\n [\n -103.85,\n 41\n ],\n [\n -103.85,\n 38\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e7835","contributors":{"authors":[{"text":"Hofstra, Warren E.","contributorId":75618,"corporation":false,"usgs":true,"family":"Hofstra","given":"Warren","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":189984,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Klein, John M.","contributorId":27036,"corporation":false,"usgs":true,"family":"Klein","given":"John","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":189985,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Major, Thomas J.","contributorId":32529,"corporation":false,"usgs":true,"family":"Major","given":"Thomas","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":189983,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":42087,"text":"ofr71291 - 1971 - Aeromagnetic map of the Challis, May, Lone Pine Peak, and Doublespring quadrangles, east-central Idaho","interactions":[{"subject":{"id":42087,"text":"ofr71291 - 1971 - Aeromagnetic map of the Challis, May, Lone Pine Peak, and Doublespring quadrangles, east-central Idaho","indexId":"ofr71291","publicationYear":"1971","noYear":false,"title":"Aeromagnetic map of the Challis, May, Lone Pine Peak, and Doublespring quadrangles, east-central Idaho"},"predicate":"SUPERSEDED_BY","object":{"id":64046,"text":"gp919 - 1978 - Aeromagnetic map of Idaho","indexId":"gp919","publicationYear":"1978","noYear":false,"title":"Aeromagnetic map of Idaho"},"id":1}],"supersededBy":{"id":64046,"text":"gp919 - 1978 - Aeromagnetic map of Idaho","indexId":"gp919","publicationYear":"1978","noYear":false,"title":"Aeromagnetic map of Idaho"},"lastModifiedDate":"2022-06-06T19:51:44.388865","indexId":"ofr71291","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"71-291","title":"Aeromagnetic map of the Challis, May, Lone Pine Peak, and Doublespring quadrangles, east-central Idaho","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr71291","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1971, Aeromagnetic map of the Challis, May, Lone Pine Peak, and Doublespring quadrangles, east-central Idaho: U.S. Geological Survey Open-File Report 71-291, 1 Plate: 29.41 x 42.51 inches, https://doi.org/10.3133/ofr71291.","productDescription":"1 Plate: 29.41 x 42.51 inches","costCenters":[],"links":[{"id":175557,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1971/0291/report-thumb.jpg"},{"id":401700,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0291/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"62500","country":"United States","state":"Idaho","otherGeospatial":"Challis Quadrangle, Doublespring Quadrangle, Lone Pine Peak Quadrangle, May Quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.8895263671875,\n 44.209772586984485\n ],\n [\n -113.7579345703125,\n 44.209772586984485\n ],\n [\n -113.7579345703125,\n 44.67646564865964\n ],\n [\n -114.8895263671875,\n 44.67646564865964\n ],\n [\n -114.8895263671875,\n 44.209772586984485\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afde4b07f02db69704b","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":530820,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1040,"text":"wsp1999D - 1971 - Underground storage of imported water in the San Gorgonio Pass area, southern California","interactions":[{"subject":{"id":55888,"text":"ofr6920 - 1969 - Underground storage of imported water in the San Gorgonio Pass area, California","indexId":"ofr6920","publicationYear":"1969","noYear":false,"title":"Underground storage of imported water in the San Gorgonio Pass area, California"},"predicate":"SUPERSEDED_BY","object":{"id":1040,"text":"wsp1999D - 1971 - Underground storage of imported water in the San Gorgonio Pass area, southern California","indexId":"wsp1999D","publicationYear":"1971","noYear":false,"chapter":"D","title":"Underground storage of imported water in the San Gorgonio Pass area, southern California"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1999D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1999","chapter":"D","title":"Underground storage of imported water in the San Gorgonio Pass area, southern California","docAbstract":"The San Gorgonio Pass ground-water basin is divided into the Beaumont, Banning, Cabazon, San Timoteo, South Beaumont, Banning Bench, and Singleton storage units. The Beaumont storage unit, centrally located in the agency area, is the largest in volume of the storage units. \r\n\r\nEstimated long-term average annual precipitation in the San Gorgonio Pass Water Agency drainage area is 332,000 acre-feet, and estimated average annual recoverable water is 24,000 acre-feet, less than 10 percent of the total precipitation. Estimated average annual surface outflow is 1,700 acre-feet, and estimated average annual ground-water recharge is 22,000 acre-feet. Projecting tack to probable steady-state conditions, of the 22.000 acre-feet of recharge, 16,003 acre-feet per year became subsurface outflow into Coachella Valley, 6,000 acre-feet into the Redlands area, and 220 acre-feet into Potrero Canyon. \r\n\r\nAfter extensive development, estimated subsurface outflow from the area in 1967 was 6,000 acre-feet into the Redlands area, 220 acre-feet into Potrero Canyon, and 800 acre-feet into the fault systems south of the Banning storage unit, unwatered during construction of a tunnel. Subsurface outflow into Coachella Valley in 1967 is probably less than 50 percent of the steady-state flow. An anticipated 17,000 .acre-feet of water per year will be imported by 1980. Information developed in this study indicates it is technically feasible to store imported water in the eastern part of the Beaumont storage unit without causing waterlogging in the storage area and without losing any significant quantity of stored water.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1999D","usgsCitation":"Bloyd, R.M., 1971, Underground storage of imported water in the San Gorgonio Pass area, southern California: U.S. Geological Survey Water Supply Paper 1999, iv, 37 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1999D.","productDescription":"iv, 37 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137996,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1999d/report-thumb.jpg"},{"id":25684,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25685,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999d/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25686,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1999d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e479fe4b07f02db49307c","contributors":{"authors":[{"text":"Bloyd, Richard M.","contributorId":55802,"corporation":false,"usgs":true,"family":"Bloyd","given":"Richard","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":143076,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3100,"text":"wsp1991 - 1971 - Quality of surface waters of the United States, 1966, Parts 1 and 2, north Atlantic slope basins and South Atlantic slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:39","indexId":"wsp1991","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1991","title":"Quality of surface waters of the United States, 1966, Parts 1 and 2, north Atlantic slope basins and South Atlantic slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1991","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1971, Quality of surface waters of the United States, 1966, Parts 1 and 2, north Atlantic slope basins and South Atlantic slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 1991, xvi, 984 p. ;23 cm., https://doi.org/10.3133/wsp1991.","productDescription":"xvi, 984 p. ;23 cm.","costCenters":[],"links":[{"id":139265,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1991/report-thumb.jpg"},{"id":30012,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1991/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db686492","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":528077,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12537,"text":"ofr7113 - 1971 - Preliminary geologic map of the Dengate quadrangle, Morton County, North Dakota","interactions":[{"subject":{"id":12537,"text":"ofr7113 - 1971 - Preliminary geologic map of the Dengate quadrangle, Morton County, North Dakota","indexId":"ofr7113","publicationYear":"1971","noYear":false,"title":"Preliminary geologic map of the Dengate quadrangle, Morton County, North Dakota"},"predicate":"SUPERSEDED_BY","object":{"id":69262,"text":"coal67 - 1974 - Geologic map and lignite deposits of the Dengate Quadrangle, Morton County, North Dakota","indexId":"coal67","publicationYear":"1974","noYear":false,"title":"Geologic map and lignite deposits of the Dengate Quadrangle, Morton County, North Dakota"},"id":1}],"supersededBy":{"id":69262,"text":"coal67 - 1974 - Geologic map and lignite deposits of the Dengate Quadrangle, Morton County, North Dakota","indexId":"coal67","publicationYear":"1974","noYear":false,"title":"Geologic map and lignite deposits of the Dengate Quadrangle, Morton County, North Dakota"},"lastModifiedDate":"2025-08-04T14:51:51.18548","indexId":"ofr7113","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"71-13","title":"Preliminary geologic map of the Dengate quadrangle, Morton County, North Dakota","docAbstract":"The Dengate quadrangle is an area of approximately 51 square miles in western Morton County, southwestern North Dakota. The quadrangle is about 40 miles west of Bismarck, the State capitol (fig. 1) and about 3.5 miles east of Glen Ullin (population 1,087). Interstate Highway 94,U.S. Highway 10, and the Northern Pacific Railroad cross the northern part of the area in an east-west direction.
The Dengate quadrangle is one of a group of 14 adjoining 71/2-minute quadrangles (fig. 1) that are being mapped by the U.S. Geological Survey to furnish a basis for classification of lands withdrawn by the Federal Government pending classification for coal, and to contribute to the geologic map atlas of the United States. Most of the fieldwork for the Dengate quadrangle was done during the late summers and early autumns of 1965 and 1966.
During the summer of 1966, the U.S. Geological Survey conducted a drilling program in the Dengate and nearby quadrangles (Smith, 1970) to gather information on the existence, thickness, and depth of lignite beds in withdrawn Federal lands. Two of the holes drilled are in the Dengate quadrangle.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr7113","usgsCitation":"Barclay, C., 1971, Preliminary geologic map of the Dengate quadrangle, Morton County, North Dakota: U.S. Geological Survey Open-File Report 71-13, Report: 31 p.; 4 Plates: 36.43 x 62.35 inches or smaller; 3 Tables: 27.37 x 25.14 inches or smaller, https://doi.org/10.3133/ofr7113.","productDescription":"Report: 31 p.; 4 Plates: 36.43 x 62.35 inches or smaller; 3 Tables: 27.37 x 25.14 inches or 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S.","affiliations":[],"preferred":false,"id":166296,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":200,"text":"wsp2011 - 1971 - Quality of surface waters of the United States, 1967, Parts 1 and 2, North Atlantic Slope basins and South Atlantic Slope and eastern Gulf of Mexico basins","interactions":[],"lastModifiedDate":"2012-02-02T00:05:10","indexId":"wsp2011","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2011","title":"Quality of surface waters of the United States, 1967, Parts 1 and 2, North Atlantic Slope basins and South Atlantic Slope and eastern Gulf of Mexico basins","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp2011","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1971, Quality of surface waters of the United States, 1967, Parts 1 and 2, North Atlantic Slope basins and South Atlantic Slope and eastern Gulf of Mexico basins: U.S. Geological Survey Water Supply Paper 2011, xvii, 982 p. ;23 cm., https://doi.org/10.3133/wsp2011.","productDescription":"xvii, 982 p. ;23 cm.","costCenters":[],"links":[{"id":136279,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2011/report-thumb.jpg"},{"id":24811,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2011/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db651981","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":527229,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2851,"text":"wsp1999F - 1971 - Prospects for developing stock - Water supplies from wells in northeastern Garfield County, Montana","interactions":[],"lastModifiedDate":"2022-12-02T21:22:05.132364","indexId":"wsp1999F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1999","chapter":"F","title":"Prospects for developing stock - Water supplies from wells in northeastern Garfield County, Montana","docAbstract":"Ground-water resources in northeastern Garfield County, Mont., afford a practical and reliable source of stock water on the intermingled public and private grazing lands that together comprise an area of about 1,200 square miles. The oldest formation exposed in the area is the relatively thick and impermeable Bearpaw Shale of Cretaceous .age. Overlying the Bearpaw Shale in succession are the Fox Hills Sandstone and Hell Creek Formation of Cretaceous age, the Fort Union Formation of Tertiary age, and thin glacial deposits .and alluvium of Quaternary age. All but the Bearpaw Shale and the glacial deposits are potential aquifers. Published geologic maps were found to be satisfactory after fitting contacts to the topographic base. Mapping, therefore, was limited mainly to outlining on aerial photographs the alluvial deposits in the stream valleys. \r\n\r\nThe major structural feature is the Blood Creek syncline, the axis of which plunges eastward 10-15 feet per mile across the southern part of the area. Beds generally dip 15-25 feet per mile toward the synclinal axis. Water in bedrock aquifers is under artesian pressure, .and most wells in Big and Little Dry Creek valleys flow at the land surface. \r\n\r\nThe only bedrock aquifer having appreciable areal extent is a sandstone 30-70 feet thick that has been mapped by previous investigators as the upper part of the Fox Hills Sandstone. This aquifer crops out in the northern and northwestern parts of the area and dips about 20 feet per mile southeastward beneath younger beds. Most wells in the northern half of the area obtain water from this sandstone at drilling depths of less than 200 feet. \r\n\r\nThe depth to the Fox Hills Sandstone increases progressively southward, and most wells south of Woody Creek obtain water from irregularly distributed sandstone beds and lenses in the overlying Hell Creek and Fort Union Formations. The depth at which water may be obtained from these beds is not accurately predictable, but the depth seldom exceeds 300 feet. \r\n\r\nThe results of the investigation indicate that the prospects for obtaining ample water for livestock from wells drilled into the bedrock formations are very favorable in most of the area. The average depth of bedrock wells in the area is 195 feet. \r\n\r\nUnderflow in the alluvial deposits along all the larger stream valleys also affords a practical source of stock water. \r\n\r\nChemical analyses of samples collected at 43 wells and three springs show the water quality to be generally poor. Water from bedrock aquifer contains 530-5,340 milligrams per liter total dissolved solids, whereas water from alluvium contains less than 1,500 milligrams per liter total dissolved solids. The predominant constituents are sodium, bicarbonate, and sulfate. So far as could be determined, all water supplies in the area are suitable for livestock.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1999F","usgsCitation":"Van Lewen, M.C., and King, N.J., 1971, Prospects for developing stock - Water supplies from wells in northeastern Garfield County, Montana: U.S. Geological Survey Water Supply Paper 1999, Report; iv, 38 p.; 1 Plate: 22.00 × 33.60 inches, https://doi.org/10.3133/wsp1999F.","productDescription":"Report; iv, 38 p.; 1 Plate: 22.00 × 33.60 inches","costCenters":[],"links":[{"id":410017,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25490.htm","linkFileType":{"id":5,"text":"html"}},{"id":29440,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1999f/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29439,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1999f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139068,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1999f/report-thumb.jpg"}],"country":"United States","state":"Montana","county":"Garfield County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -106.17,\n 47.941\n ],\n [\n -107.012,\n 47.941\n ],\n [\n -107.012,\n 47.151\n ],\n [\n -106.17,\n 47.151\n ],\n [\n -106.17,\n 47.941\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a92e4b07f02db657bdb","contributors":{"authors":[{"text":"Van Lewen, M. C.","contributorId":33574,"corporation":false,"usgs":true,"family":"Van Lewen","given":"M.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":145906,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"King, Norman Julius","contributorId":57048,"corporation":false,"usgs":true,"family":"King","given":"Norman","email":"","middleInitial":"Julius","affiliations":[],"preferred":false,"id":145907,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":6133,"text":"pp665 - 1971 - Geology and mineral deposits, east flank of the Elkhorn Mountains, Broadwater County, Montana","interactions":[{"subject":{"id":47214,"text":"ofr68303 - 1968 - Geologic map of the east flank of the Elkhorn Mountains, Broadwater County, Montana","indexId":"ofr68303","publicationYear":"1968","noYear":false,"title":"Geologic map of the east flank of the Elkhorn Mountains, Broadwater County, Montana"},"predicate":"SUPERSEDED_BY","object":{"id":6133,"text":"pp665 - 1971 - Geology and mineral deposits, east flank of the Elkhorn Mountains, Broadwater County, Montana","indexId":"pp665","publicationYear":"1971","noYear":false,"title":"Geology and mineral deposits, east flank of the Elkhorn Mountains, Broadwater County, Montana"},"id":1}],"lastModifiedDate":"2025-09-23T17:11:02.96343","indexId":"pp665","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","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":"665","title":"Geology and mineral deposits, east flank of the Elkhorn Mountains, Broadwater County, Montana","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp665","usgsCitation":"Klepper, M.R., Ruppel, E.T., Freeman, V.L., and Weeks, R.A., 1971, Geology and mineral deposits, east flank of the Elkhorn Mountains, Broadwater County, Montana: U.S. Geological Survey Professional Paper 665, Report: iv, 66 p.: 4 Plates: 29.17 x 45.44 inches or smaller, https://doi.org/10.3133/pp665.","productDescription":"Report: iv, 66 p.: 4 Plates: 29.17 x 45.44 inches or smaller","costCenters":[],"links":[{"id":112714,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0665/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":112713,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0665/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":112712,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0665/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":112711,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0665/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":112710,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0665/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":495916,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4987.htm","linkFileType":{"id":5,"text":"html"}},{"id":140348,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0665/report-thumb.jpg"}],"country":"United States","state":"Montana","county":"Broadwater County","otherGeospatial":"Elkhorn Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -111.75,\n 46.5\n ],\n [\n -111.75,\n 46.125\n ],\n [\n -111.625,\n 46.125\n ],\n [\n -111.625,\n 46.5\n ],\n [\n -111.75,\n 46.5\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db685138","contributors":{"authors":[{"text":"Klepper, Montis Ruhl","contributorId":27431,"corporation":false,"usgs":true,"family":"Klepper","given":"Montis","email":"","middleInitial":"Ruhl","affiliations":[],"preferred":false,"id":152175,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ruppel, E. T.","contributorId":6041,"corporation":false,"usgs":true,"family":"Ruppel","given":"E.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":152174,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Freeman, V. L.","contributorId":52958,"corporation":false,"usgs":true,"family":"Freeman","given":"V.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":152176,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Weeks, R. A.","contributorId":75914,"corporation":false,"usgs":true,"family":"Weeks","given":"R.","middleInitial":"A.","affiliations":[],"preferred":false,"id":152177,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":42666,"text":"ofr7188 - 1971 - Regional geologic map of San Andreas and related faults in eastern San Gabriel Mountains, San Bernardino Mountains, western San Jacinto Mountains and vicinity, Los Angeles, San Bernardino, and Riverside Counties, California","interactions":[],"lastModifiedDate":"2022-06-14T21:43:19.482801","indexId":"ofr7188","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"71-88","title":"Regional geologic map of San Andreas and related faults in eastern San Gabriel Mountains, San Bernardino Mountains, western San Jacinto Mountains and vicinity, Los Angeles, San Bernardino, and Riverside Counties, California","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr7188","usgsCitation":"Dibblee, T.W., 1971, Regional geologic map of San Andreas and related faults in eastern San Gabriel Mountains, San Bernardino Mountains, western San Jacinto Mountains and vicinity, Los Angeles, San Bernardino, and Riverside Counties, California: U.S. Geological Survey Open-File Report 71-88, 1 Plate: 65.00 × 34.00 inches, https://doi.org/10.3133/ofr7188.","productDescription":"1 Plate: 65.00 × 34.00 inches","costCenters":[],"links":[{"id":176613,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":98923,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1971/0088/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":402189,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8666.htm"}],"scale":"250000","country":"United States","state":"California","county":"Los Angeles County, Riverside County, San Bernardino County","otherGeospatial":"San Andreas and related faults","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.421630859375,\n 33.75174787568194\n ],\n [\n -117.158203125,\n 33.75174787568194\n ],\n [\n -117.158203125,\n 34.59251960889388\n ],\n [\n -118.421630859375,\n 34.59251960889388\n ],\n [\n -118.421630859375,\n 33.75174787568194\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a60e4b07f02db634fe1","contributors":{"authors":[{"text":"Dibblee, T. W. Jr.","contributorId":95445,"corporation":false,"usgs":true,"family":"Dibblee","given":"T.","suffix":"Jr.","middleInitial":"W.","affiliations":[],"preferred":false,"id":226905,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70197572,"text":"70197572 - 1971 - The earthquake sequence near Danville, California, 1970","interactions":[],"lastModifiedDate":"2023-10-29T16:06:33.844958","indexId":"70197572","displayToPublicDate":"1971-12-31T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1135,"text":"Bulletin of the Seismological Society of America","onlineIssn":"1943-3573","printIssn":"0037-1106","active":true,"publicationSubtype":{"id":10}},"title":"The earthquake sequence near Danville, California, 1970","docAbstract":"Several thousand small earthquakes, with magnitudes ranging up to 4, occurred near Danville, California, during May, June, and July 1970. Seven temporary seismographs were installed near the epicentral region to augment an existing telemetered network within 1 day after the first felt earthquake. The dense concentration of 10 seismographs within 12 km of the seismic activity and the existence of a reversed seismic-refraction profile through the region permitted a very detailed study of this earthquake sequence. Over 400 events with magnitude greater than 0.5 were located with an average accuracy of ±1 km. The main earthquake region was approximately spherical: 1 km in radius, 6 km deep, and centered about 5 km southeast of Danville, 40 km east of San Francisco. Fault-plane solutions indicate that faulting associated with the earthquakes was of the right-lateral strike-slip type, with a strike of N 35°W.
","language":"English","publisher":"Seismological Society of America","doi":"10.1785/BSSA0610061771","usgsCitation":"Lee, W., Eaton, M., and Brabb, E.E., 1971, The earthquake sequence near Danville, California, 1970: Bulletin of the Seismological Society of America, v. 61, no. 6, p. 1771-1794, https://doi.org/10.1785/BSSA0610061771.","productDescription":"24 p.","startPage":"1771","endPage":"1794","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":354943,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Danville","otherGeospatial":"San Francisco Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.17596435546876,\n 36.92793899776678\n ],\n [\n -121.47857666015625,\n 36.92793899776678\n ],\n [\n -121.47857666015625,\n 38.417014454352035\n ],\n [\n -123.17596435546876,\n 38.417014454352035\n ],\n [\n -123.17596435546876,\n 36.92793899776678\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"61","issue":"6","noUsgsAuthors":false,"publicationDate":"1971-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Lee, W.H.K.","contributorId":35303,"corporation":false,"usgs":true,"family":"Lee","given":"W.H.K.","affiliations":[],"preferred":false,"id":737723,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Eaton, M.S.","contributorId":205553,"corporation":false,"usgs":false,"family":"Eaton","given":"M.S.","email":"","affiliations":[],"preferred":false,"id":737724,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brabb, E. E.","contributorId":43780,"corporation":false,"usgs":true,"family":"Brabb","given":"E.","middleInitial":"E.","affiliations":[],"preferred":false,"id":737725,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70197780,"text":"70197780 - 1971 - Structural implications of an offset Early Cretaceous shoreline in northern California","interactions":[],"lastModifiedDate":"2018-06-20T09:30:09","indexId":"70197780","displayToPublicDate":"1971-12-31T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Structural implications of an offset Early Cretaceous shoreline in northern California","docAbstract":"Recognition of a nonmarine to marine transition in sedimentary rocks at Glade Creek and Big Bar in the southern Klamath Mountains permits reconstruction of the approximate position of a north-trending Early Cretaceous (Valanginian) shoreline. At the southern end of the Klamath Mountains, the shoreline is displaced 60 mi or more to the east by a west-northwest-trending fault zone. South of this fault zone the shoreline is buried at a much lower level beneath late Cenozoic rocks in the Great Valley. This large displacement probably is the result of differential movement along a system of left-lateral tear faults in the upper plate of the Coast Range thrust. The westward bulge of the Klamath arc also may have resulted from this faulting, as the amount and direction of the bulge is comparable with the displacement of the Valanginian shoreline.
Basal clastic strata at both Glade Creek and Big Bar contain abundant fresh-water or brackish-water clams, many of which consist of unabraded paired valves. These are conformably overlain by Valanginian marine strata containing Buchia crassicollis solida.
The position of the Valanginian shoreline beneath the Great Valley cannot be directly observed because it is buried by thick late Cenozoic deposits. However, its approximate westernmost limit must lie between the outcrop belt of marine strata on the west side of the valley and drill holes to basement on the east side, in which equivalent strata are absent.
Franciscan rocks containing Valanginian fossils occur 10 mi southwest of Glade Creek, but these are deep-water marine eugeosynclinal rocks that were deposited far to the west of the shoreline. The deformation responsible for the displacement of the Valanginian shoreline and juxtaposition of the Franciscan rocks and Klamath Mountain basement rocks involved eastward under-thrusting of the Franciscan beneath the Coast Range thrust contemporaneous with differential movement along tear faults within the upper plate.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1971)82[815:SIOAOE]2.0.CO;2","usgsCitation":"Jones, D.L., and Irwin, W., 1971, Structural implications of an offset Early Cretaceous shoreline in northern California: GSA Bulletin, v. 82, p. 815-822, https://doi.org/10.1130/0016-7606(1971)82[815:SIOAOE]2.0.CO;2.","productDescription":"8 p.","startPage":"815","endPage":"822","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":355193,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","volume":"82","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Jones, D. L.","contributorId":65045,"corporation":false,"usgs":true,"family":"Jones","given":"D.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":738474,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Irwin, W. P.","contributorId":82347,"corporation":false,"usgs":true,"family":"Irwin","given":"W. P.","affiliations":[],"preferred":false,"id":738475,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207545,"text":"70207545 - 1971 - Origin of the differentiated and hybrid lavas of Kilauea Volcano, Hawaii","interactions":[],"lastModifiedDate":"2020-06-03T15:51:26.883042","indexId":"70207545","displayToPublicDate":"1971-12-23T11:33:47","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2420,"text":"Journal of Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Origin of the differentiated and hybrid lavas of Kilauea Volcano, Hawaii","docAbstract":"Kilauea Volcano has erupted lava from its summit caldera and from two rift zones that extend from the summit towards the east and south-west. Lavas erupted from the summit of the volcano differ from each other principally in their content of olivine and define lines of ‘olivine control’ on magnesia variation diagrams. Lavas erupted on the rift zones may be similar in composition to the summit lavas or may be differentiated by processes that involve minerals other than olivine. All of the differentiated lavas have less than 6·8 per cent MgO and plot off the extension of olivine control lines for the summit lavas. Prehistoric vents (before A.D. 1750) from which differentiated lavas have been erupted are found on the east rift zone and in the western Koae fault zone adjacent to the south-west rift zone; historic vents for differentiated lavas are confined to the east rift zone. Twenty-one new analyses are presented for several of the east rift differentiates and for the newly discovered differentiates adjacent to the south-west rift zone. The differentiates have MgO as low as 3·9 per cent and SiO2 as high as 56 per cent; both extremes are found in the prehistoric lavas adjacent to the south-west rift.
Detailed petrochemical studies suggest the following conclusions:
The chemical composition of magma erupted at Kilauea summit varies with the date of eruption. Lavas erupted before 1750, during the eighteenth and nineteenth centuries, and in the twentieth century form groups that can be distinguished chemically. On a lesser scale, each Kilauea summit eruption in the twentieth century has a chemistry that is distinctive with respect to the chemistry of every other summit eruption.
During late prehistoric time pockets of differentiated magma were formed within the rift zones by separation of the liquid remaining after partial crystallization of bodies of summit magma. This process presumably is still going on within the east rift zone, but the more recently separated liquids have not yet been erupted to the surface. The relative time at which these differentiated magmas were produced can be estimated from calculations based on their chemical compositions, which show that the differentiates could lie on the liquid line of descent for Kilauea summit magma of prehistoric composition but not on any liquid line of descent for younger summit magmas.
Lava from some eruptions, notably the early part of the 1955 eruption on the lower east rift, has the composition of the liquid fraction as it is generated within the rift. Lava compositions of other eruptions, including those of the later lavas of 1955, are best explained by mixing of magma supplied from a central reservoir beneath Kilauea summit with the differentiated liquid in the rift. Lava from each summit eruption is unique chemically, so it is possible to recognize its presence or absence as components of mixing in such mixed lavas. It appears that summit magma of composition characteristic of the 1952 and 1961 Halemaumau eruptions contributed to the composition of the mixed lavas produced in the latter part of the 1955 eruption. Summit magma of 1961 composition is alone sufficient to explain the composition of mixed lavas erupted in 1960 and 1961. In rift lavas erupted from 1962 to 1965, the composition of lava erupted in Halemaumau in 1967, in addition to the 1961 composition, is a component of mixing, and it is the dominant summit component in the composition of the two 1965 eruptions. The proportion of summit magma to differentiated magma needed to explain the composition of lavas erupted on the upper east rift increases from 1961 to 1965; this increase indicates that the differentiated magma was being diluted and used up by repeated flooding of this part of the rift zone by magma supplied from the central reservoir.
The fact that components of ‘summit composition’ appear in rift eruptions before they appear undiluted in Halemaumau suggests that the central reservoir is vertically zoned. Rift eruptions are fed from lower levels where younger magma is available, and summit eruptions are fed from the relatively older magma above. The chemical distinction between lava of successive summit eruptions implies that significant convective mixing of magma does not take place throughout the central reservoir.
The unique and uniform composition of lava of each successive summit eruption also suggests that summit eruptions end when all of the magma of one composition has been erupted. The magma erupted from the upper levels of the reservoir during one cycle is continually replaced from below by younger magma of different composition. In order for eruption to be renewed in Halemaumau, new magma from the mantle must be held in storage at intermediate levels before it attains an ‘eruptive state’.
The hypothesis presented in 2–4 above permits qualitative predictions concerning future lava compositions. The composition of the next lava to be erupted in Halemaumau is expected to be distinct from that of the 1967 eruption, and this composition will presumably be identified in rift eruptions occurring between 1967 and the time of its appearance in Halemaumau.
Differentiates of prehistoric age also were apparently formed in the same way as those of historic age, but the mixing cannot be described quantitatively because of poor control on the stratigraphy and the compositions of erupted lavas. One lava in the Koae group, that from Yellow Cone, appears to be a mixture of a picritic magma (12 per cent MgO) with a differentiated liquid with less than 2·5 per cent MgO and nearly 60 per cent SiO2.
This report discusses the results of aeromagnetic survey bounded by latitudes 45°30′ N. and 47°00′ N. and extending from the Rocky Mountains, to approximately 120 mi offshore in the Pacific Ocean. East of the Rocky Mountains, a larger area has been surveyed in the Great Plains bounded approximately by latitudes 44°50′ N. and 48°10′ N. and by longitudes 104°W. and 110°W.
Throughout the area of the survey, the magnetic map is marked by conspicuous northeast and northwest anomaly trends, lineaments, and breaks in the anomaly pattern. Their regional distribution, over-all magnetic character, and geologic evidence suggest that they are major structural features in the basement rocks. The close correspondence of structural and geologic features in younger rocks with these basement magnetic and structural trends suggest that basement trends controlled or at least greatly influenced intrusion, deposition, and structural history of younger rocks. In some cases, evidence suggests that basement structures have been reactivated during later tectonic activity.
Perhaps even more striking than the northeast- and northwest-trending features are large east-west magnetic discontinuities which, in some cases, extend completely across the strip to the edge of the shelf, and which, in some cases, can be correlated with large-scale discontinuities dating back to the Precambrian.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1971)82[3347:IOAASA]2.0.CO;2","usgsCitation":"Zietz, I., Hearn, B.C., Higgins, M.W., Robinson, G.D., and Swanson, D., 1971, Interpretation of an aeromagnetic strip across the northwestern United States: Bulletin of the Geological Society of America, v. 82, no. 12, p. 3347-3372, https://doi.org/10.1130/0016-7606(1971)82[3347:IOAASA]2.0.CO;2.","productDescription":"26 p.","startPage":"3347","endPage":"3372","costCenters":[],"links":[{"id":394358,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho, Montana, North Dakota, Oregon, South Dakota, Washington, Wyoming","otherGeospatial":"Pacific Ocean, Rocky Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -125.068359375,\n 45.5\n ],\n [\n -103.3937890625,\n 45.5\n ],\n [\n -103.3937890625,\n 47.0\n ],\n [\n -125.068359375,\n 47.0\n ],\n [\n -125.068359375,\n 45.5\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"82","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":830781,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hearn, B. Carter chearn@usgs.gov","contributorId":189844,"corporation":false,"usgs":true,"family":"Hearn","given":"B.","email":"chearn@usgs.gov","middleInitial":"Carter","affiliations":[],"preferred":true,"id":830782,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Higgins, Michael W.","contributorId":12459,"corporation":false,"usgs":true,"family":"Higgins","given":"Michael","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":830783,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Robinson, G. D.","contributorId":96669,"corporation":false,"usgs":true,"family":"Robinson","given":"G.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":830784,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Swanson, Donald A. 0000-0002-1680-3591","orcid":"https://orcid.org/0000-0002-1680-3591","contributorId":229682,"corporation":false,"usgs":true,"family":"Swanson","given":"Donald A.","affiliations":[],"preferred":true,"id":830785,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70227455,"text":"70227455 - 1971 - Upper Cenozoic basalts with high Sr87/Sr86 and Sr/Rb ratios, southern Great Basin, western United States","interactions":[],"lastModifiedDate":"2022-01-17T19:40:53.91535","indexId":"70227455","displayToPublicDate":"1971-12-01T13:35:57","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Upper Cenozoic basalts with high Sr87/Sr86 and Sr/Rb ratios, southern Great Basin, western United States","title":"Upper Cenozoic basalts with high Sr87/Sr86 and Sr/Rb ratios, southern Great Basin, western United States","docAbstract":"Upper Cenozoic basalts from southwestern Nevada and east-central California are unusually rich in both strontium (~ 1,200 ppm) and Sr87 (initial Sr87/Sr86 ~ 0.707). The average Rb/Sr ratio of these basalts is too low to have generated the observed Sr87/Sr86 ratio during the 4.6 b.y. of the Earth's existence, and the high strontium contents and low Rb/Sr ratios effectively rule out introduction to the basalts of the high Sr87/Sr86 values through contamination by more radiogenic material during ascent through the crust. Instead, the basalts must have been derived from unusual mantle material in which an originally high Rb/Sr ratio was markedly lowered during an earlier phase of magmatic activity.
Variations in the ratio of K2O to SiO2 in andesitic rocks suggest early and middle Cenozoic subduction beneath the western United States along two subparallel imbricate zones dipping about 20 degrees eastward. The western zone emerged at the continental margin, but the eastern zone was entirely beneath the continental plate. Mesozoic subduction apparently occurred along a single steeper zone.
","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.174.4011.821","issn":"00368075","usgsCitation":"Lipman, P.W., Prostka, H., and Christiansen, R., 1971, Evolving subduction zones in the western United States, as interpreted from igneous rocks: Science, v. 174, no. 4011, p. 821-825, https://doi.org/10.1126/science.174.4011.821.","productDescription":"5 p.","startPage":"821","endPage":"825","costCenters":[],"links":[{"id":219229,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"western United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -126.74221709761946,\n 48.97652831180986\n ],\n [\n -126.74221709761946,\n 31.724368695952563\n ],\n [\n -103.42282726016703,\n 31.724368695952563\n ],\n [\n -103.42282726016703,\n 48.97652831180986\n ],\n [\n -126.74221709761946,\n 48.97652831180986\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"174","issue":"4011","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0d94e4b0c8380cd530c9","contributors":{"authors":[{"text":"Lipman, P. W.","contributorId":93470,"corporation":false,"usgs":true,"family":"Lipman","given":"P.","middleInitial":"W.","affiliations":[],"preferred":false,"id":358694,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Prostka, H.J.","contributorId":31369,"corporation":false,"usgs":true,"family":"Prostka","given":"H.J.","affiliations":[],"preferred":false,"id":358693,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Christiansen, R.L. 0000-0002-8017-3918","orcid":"https://orcid.org/0000-0002-8017-3918","contributorId":25565,"corporation":false,"usgs":true,"family":"Christiansen","given":"R.L.","affiliations":[],"preferred":false,"id":358692,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5220426,"text":"5220426 - 1971 - A starling-deterrent wood duck nest box","interactions":[],"lastModifiedDate":"2025-02-20T22:35:22.567121","indexId":"5220426","displayToPublicDate":"1971-10-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2508,"text":"Journal of Wildlife Management","active":true,"publicationSubtype":{"id":10}},"title":"A starling-deterrent wood duck nest box","docAbstract":"In many parts of the United States, the starling (Sturnus vulgaris) has I become a serious competitor for nest boxes erected for wood ducks (Aix sponsa). Research at the Patuxent Wildlife Research Center and at Eastern Neck National Wildlife Refuge near Rock Hall, Maryland, demonstrated that horizontal nest structures with semicircular entrance holes 11 inches in diameter were acceptable to nesting wood ducks but discouraged nesting by starlings. Starlings seemed to prefer boxes in open impoundments to those in wooded impoundments, whereas wood ducks seemed to show no preference.
","language":"English","publisher":"Wiley","doi":"10.2307/3799789","usgsCitation":"McGilvrey, F., and Uhler, F.M., 1971, A starling-deterrent wood duck nest box: Journal of Wildlife Management, v. 35, no. 4, p. 793-797, https://doi.org/10.2307/3799789.","productDescription":"5 p.","startPage":"793","endPage":"797","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":196260,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Maryland","otherGeospatial":"Patuxent Wildlife Research Center","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -76.82185591899788,\n 39.07802646798717\n ],\n [\n -76.82185591899788,\n 38.98396548979565\n ],\n [\n -76.71643624290974,\n 38.98396548979565\n ],\n [\n -76.71643624290974,\n 39.07802646798717\n ],\n [\n -76.82185591899788,\n 39.07802646798717\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"35","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a6323","contributors":{"authors":[{"text":"McGilvrey, Frank B.","contributorId":14908,"corporation":false,"usgs":true,"family":"McGilvrey","given":"Frank B.","affiliations":[],"preferred":false,"id":331796,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Uhler, Francis M.","contributorId":49838,"corporation":false,"usgs":true,"family":"Uhler","given":"Francis","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":331797,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70227391,"text":"70227391 - 1971 - Relations of folded dikes and Precambrian polyphase deformation, Gardner Lake area, Beartooth Mountains, Wyoming","interactions":[],"lastModifiedDate":"2022-01-12T20:01:25.112754","indexId":"70227391","displayToPublicDate":"1971-08-01T13:51:32","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Relations of folded dikes and Precambrian polyphase deformation, Gardner Lake area, Beartooth Mountains, Wyoming","docAbstract":"Two cross-cutting mafic dikes in the headwall of Gardner Lake in the eastern Beartooth Mountains, Wyoming, have structural relations with Archean migmatite and gneiss that suggest intrusion between deformational phases recognized in the eastern part of the range. Fabric data show that the older dike, an orthoamphibolite, was emplaced subsequent to the F1 deformational event, but prior to the main episode of metamorphism, metasomatism, and folding, F2. The younger dike, a metanorite, was intruded after F2, but is folded by west-trending, open F3 folds. The style and general trend of these F3 folds are consistent with those observed elsewhere in the eastern part of the range. The data available and absolute age relations in other parts of the range indicate that F2 occurred 2750 m.y. ago and F3 1600 to 1800 m.y. ago.
All early students of the zinc and barite deposits of East Tennessee, noting the geographic coincidence of the principal mining area with complex late Paleozoic geologic structure, concluded that (1) the ore-bearing breccias were produced by Appalachian tectonic forces and that (2) mineralizing solutions gained access through fault-produced channelways. In 1931, Ulrich suggested that the breccias were produced by collapse and fragmentation resulting from solution of the carbonate rocks. This idea was promptly rejected by most geologists, and for the next 15 years nearly all papers on these deposits contained refutations of Ulrich's hypothesis and \"proof\" of the late Paleozoic tectonic origin of the breccias. Recognition by Odell in 1950 of a spatial association between thinning of the lime-stone zone of the Kingsport Formation and the presence of ore bodies, plus the observation that all identifiable blocks in the breccias were displaced downward as much as 30 to 50 feet, led him to suggest that foundering of the rocks over solution-thinned zones produced the breccias. Hydrothermal fluids, rather than ordinary ground water, were thought to be the dissolving agent.Kendall, in 1960, described a stratified \"varved\" matrix with detrital sphalerite grains in many breccias at Jefferson City, in which lamination is parallel to bedding of the host Kingsport Formation, indicating that both brecciation and mineralization occurred while the rocks were horizontal. Ruskell about 1960 pointed out the similarity between cross sections of southwest Wisconsin ore bodies and those of East Tennessee when the latter were rotated to a horizontal position. Detailed studies of the post-Knox unconformity led to recognition of a paleokarst topography of considerable relief developed on this surface. Regional stratigraphic studies of the Knox Group by Harris demonstrated the probability of pre-Middle Ordovician exposure of the Kingsport somewhere to the north or northwest, providing a recharge area for ground waters at that time. Detailed mapping of ore bodies, barren areas, and related structures by the mining-company geologists, plus application of the principles of ground-water hydrology and rock mechanics, has led to the theory, generally accepted in the district, of solution-collapse origin of the breccias, probably during Ordovician time.
Based on a study of minor occurrences of zinc, barite, and iron in East Tennessee, certain deposits are interpreted to have formed during early Middle Ordovician time. Principal lines of evidence supporting this age are: (1) the occurrence of barite, sphalerite, and pyrite associated with synsedimentary collapse breccias which span the pre-Middle Ordovician unconformity at the Lost Creek barite mine in Union County; (2) barite in basal Middle Ordovician beds (Athens Shale and Lenoir Limestone) in northeastern Tennessee and southwestern Virginia; (3) sphalerite and pyrite in dolomite filling paleocaves in the uppermost part of the Lower Ordovician Mascot Dolomite at the Trotter prospect near Douglas Dam in Sevier County; and (4) oolitic hematite and pyritiferous beds near the base of the Athens Shale and subjacent pyritiferous collapse breccias in the Mascot and Kingsport Formations at several localities along the eastern side of the Appalachian Valley. Thus, it is concluded that ascending solutions formed epigenetic deposits in pre-Middle Ordovician carbonate strata nearly contemporaneously with syngenetic deposits in early Middle Ordovician sediments. These findings are in general accord with those of recent workers in the Mascot-Jefferson City and Copper Ridge districts who have proposed that mineralization in these areas occurred during the time interval of pre-Middle Ordovician erosion. The long-held theory which associates mineralization with late Paleozoic diastrophism is not supported.
","language":"English","publisher":"Society of Economic Geologists ","doi":"10.2113/gsecongeo.66.5.792","issn":"03610128","usgsCitation":"Carpenter, R., Fagan, J., and Wedow, H., 1971, Evidence on the age mineralization in the of east of barite, zinc, and iron lower paleozoic rocks Tennessee: Economic Geology, v. 66, no. 5, p. 792-798, https://doi.org/10.2113/gsecongeo.66.5.792.","productDescription":"7 p. 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Jr.","contributorId":6369,"corporation":false,"usgs":true,"family":"Wedow","given":"H.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":776938,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70207135,"text":"70207135 - 1971 - An early middle ordovician age for collapse breccias in the east Tennessee zinc districts as indicated by compaction and porosity features","interactions":[],"lastModifiedDate":"2019-12-09T09:28:15","indexId":"70207135","displayToPublicDate":"1971-08-01T09:22:37","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"An early middle ordovician age for collapse breccias in the east Tennessee zinc districts as indicated by compaction and porosity features","docAbstract":"The carbonate strata of the Lower Ordovician formations in the southern Appalachian Valley were probably considerably thicker, less compacted, and more porous and permeable in early Middle Ordovician time than they are now. Analysis of selected compaction features of rocks associated with the breccias of the East Tennessee zinc districts permits quantitative estimation of the relative compaction (reduction in thickness) these sediments have undergone before and after brecciation. Total reduction in thickness of certain Lower Ordovician marker beds because of compaction during burial under younger Paleozoic sedimentary rocks and imbricate Appalachian thrust sheets appears to be at least some 40 to 50 percent. Furthermore, it is also estimated that about half of this compaction took place after brecciation in the solution-collapse structures of the zinc deposits. In comparison with laboratory compaction tests on carbonate muds it is apparent that the Lower Ordovician rocks had been buried to a depth of at least several thousand feet by the end of the Paleozoic Era. On the other hand the zones of collapse breccias probably formed at depths of generally less than a thousand feet, thus indicating an early Middle Ordovician age for their development. The general character of the rock during this time probably was similar to that of Tertiary limestone, which acts as the principal aquifer in the Coastal Plain region of southeastern United States.
","language":"English","publisher":"Society for Economic Geologists ","doi":"10.2113/gsecongeo.66.5.725","issn":"03610128","usgsCitation":"Hill, W.T., and Wedow, H., 1971, An early middle ordovician age for collapse breccias in the east Tennessee zinc districts as indicated by compaction and porosity features: Economic Geology, v. 66, no. 5, p. 725-734, https://doi.org/10.2113/gsecongeo.66.5.725.","productDescription":"10 p. 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\"}}]}","volume":"66","issue":"5","noUsgsAuthors":false,"publicationDate":"1971-08-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hill, W. T.","contributorId":221078,"corporation":false,"usgs":false,"family":"Hill","given":"W.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":776933,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wedow, H. Jr.","contributorId":6369,"corporation":false,"usgs":true,"family":"Wedow","given":"H.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":776934,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70227158,"text":"70227158 - 1971 - Problems on the origin of ore deposits in the lower Ordovician formations of east Tennessee","interactions":[],"lastModifiedDate":"2021-12-31T15:05:36.448981","indexId":"70227158","displayToPublicDate":"1971-08-01T08:53:36","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Problems on the origin of ore deposits in the lower Ordovician formations of east Tennessee","docAbstract":"Most recent workers in the East Tennessee zinc and barite districts are in general agreement that the host breccias were formed by solution-collapse processes in early Middle Ordovician time, probably in an ancient carbonate aquifer system of regional extent. There is little agreement, however, on the source and nature of the ore fluids from which the epigenetic minerals were formed. In this symposium Hanshaw and his colleagues have presented evidence in support of the concept that much secondary dolomite may have been formed by ground water. On the other hand, Roedder has shown that fluid inclusion studies indicate hot saline brines (75 degrees -150 degrees C) as the source fluids for the ore minerals, and he suggests that they may have been deeply circulating connate brines. Other investigators in the past have proposed a variety of source fluids, including juvenile waters, meteoric waters that have become enriched by the leaching of particular elements from the surrounding rock, and sea water.
In the zinc deposits, sphalerite is accompanied locally by minor amounts of galena and pyrite, and occasionally, traces of chalcopyrite. Dolomite is the chief gangue mineral and is associated with lesser amounts of quartz, calcite, barite, fluorite, anhydrite, gypsum, and bitumen. Some deposits containing barite as the dominant ore mineral have various amounts of fluorite and pyrite; sphalerite and galena may be present locally along with the other gangue minerals typical of the zinc deposits. The paragenetic sequences of the minerals have been determined for most of the mines and many of the prospects, and, except for minor refinements, will be little changed by additional studies. The real problem, though, is the correlation of these depositional sequences from mine to mine and from district to district. Perhaps the major difficulty in the correlation is the seemingly uncomplicated mineralogy that disguises a rather complex regional paragenesis.
Questions regarding the routes the ore fluids travelled to reach the sites of deposition, the reasons why the ores are concentrated in some areas more than others, and the reasons why the mineralogy varies from area to area are questions that are unanswered or at best only partly answered. Studies to date have produced convincing evidence concerning the nature of the structures and the physical conditions responsible for the localization of ore in the Kingsport Formation (Lower Ordovician). On the other hand, the relation of the Kingsport ores to the smaller deposits in the underlying Lower Ordovician and Cambrian rocks is but little understood, and no final answer to the origin of these deposits can be reached until this relationship has been satisfactorily explained.
Fluid inclusion studies, trace element analysis, and isotopic studies of all sorts are needed to further our understanding of these seemingly simple ores. Continued detailed studies of field relations, both regional and local, are of major importance, not only for what they will reveal in themselves, but also to perfect the frames of reference in which to place the growing mass of laboratory data.
Approximately 1,330 fluid inclusions were studied in samples of ore and gangue minerals from both massive ore and late-stage vugs from a series of Appalachian deposits and five active mines in the East Tennessee zinc districts. Most primary inclusions in sphalerite, fluorite, dolomite, and quartz from East Tennessee homogenized at 82 degrees -149 degrees C. Most primary inclusions in fluorite, barite, and sphalerite from the Central Kentucky, Central Tennessee, and Sweetwater barite districts, ranged from 72 degrees -132 degrees C. Pressure corrections to be added are probably less than 10 degrees C.Freezing data were obtained as a crude measure of the salinity of the inclusion fluids. With few exceptions, all primary inclusions contained very strongly saline brines (mostly >20 weight percent salts), with appreciable amounts of at least some salts other than NaCl, and some contained immiscible globules of oil. The exceptions include several quartz, fluorite, calcite, and barite samples that contained only moderately saline brines (12-16 percent), and some inclusions containing essentially fresh water, in vug calcite. Secondary inclusions had lower salinities than adjacent primaries. Eight primary inclusions in the differently colored outer millimeter of one Central Kentucky fluorite had low salinity (4-6 percent).The data indicate that all these deposits formed from hot, saline brines, with sphalerite forming from slightly hotter and more saline fluids than later gangue minerals. This places severe restrictions on possible modes of origin and makes deeply circulating connate brines the most probable ore fluids. The data give no information on the cause or direction of fluid circulation, which would be controlled by topography, salinity, and temperature during ore deposition, and they permit wide latitude in the construction of possible models. Other observations, on \"colloform\" textures, seem to indicate the admixture of at least small amounts of surface waters with the brines.