No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp621","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1968, Aeromagnetic map of the East Brookfield quadrangle, Worcester County, Massachusetts: U.S. Geological Survey Geophysical Investigations Map 621, 1 Plate: 25.24 x 28.41 inches, https://doi.org/10.3133/gp621.","productDescription":"1 Plate: 25.24 x 28.41 inches","costCenters":[],"links":[{"id":250308,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0621/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":490887,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_5988.htm","linkFileType":{"id":5,"text":"html"}},{"id":250309,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0621/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":253802,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0621/report-thumb.jpg"}],"scale":"24000","country":"United States","state":"Massachusetts","county":"Worcester County","otherGeospatial":"East Brookfield quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -72.125,\n 42.25\n ],\n [\n -72.125,\n 42.125\n ],\n [\n -72,\n 42.125\n ],\n [\n -72,\n 42.25\n ],\n [\n -72.125,\n 42.25\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db6969b8","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":533421,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52597,"text":"ofr67125 - 1968 - Ground-water resources in the vicinity of the Crown Point Fish Hatchery, Essex County, New York","interactions":[{"subject":{"id":52597,"text":"ofr67125 - 1968 - Ground-water resources in the vicinity of the Crown Point Fish Hatchery, Essex County, New York","indexId":"ofr67125","publicationYear":"1968","noYear":false,"title":"Ground-water resources in the vicinity of the Crown Point Fish Hatchery, Essex County, New York"},"predicate":"SUPERSEDED_BY","object":{"id":70046987,"text":"70046987 - 1968 - Ground-water resources in the vicinity of the Crown Point fish hatchery, Essex County, New York","indexId":"70046987","publicationYear":"1968","noYear":false,"title":"Ground-water resources in the vicinity of the Crown Point fish hatchery, Essex County, New York"},"id":1}],"supersededBy":{"id":70046987,"text":"70046987 - 1968 - Ground-water resources in the vicinity of the Crown Point fish hatchery, Essex County, New York","indexId":"70046987","publicationYear":"1968","noYear":false,"title":"Ground-water resources in the vicinity of the Crown Point fish hatchery, Essex County, New York"},"lastModifiedDate":"2016-02-08T09:07:04","indexId":"ofr67125","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"67-125","title":"Ground-water resources in the vicinity of the Crown Point Fish Hatchery, Essex County, New York","docAbstract":"The Crown Point Fish Hatchery, one of several hatcheries operated by the New York State Conservation Department, is located in Crown Point Center, Essex County, on the eastern edge of the Adirondack Highlands and about 2 miles west of Lake Champlain. Figure 1 is a location map of the vicinity of the Hatchery. This report summarizes an investigation by the U.S. ·Geological Survey, in cooperation with the New York State Conservation Department, Division of Water Resources, to locate and evaluate sources of additional ground-water supply for the Hatchery. In order to expand the facilities at the Hatchery, an additional water supply of about 100 gpm (gallons per minute) to as much as 350 gpm is needed. In addition, the type of fish culture practiced requires a water temperature of about 7 to 13 degrees Celsius (centigrade) for optimum results.
\nThe cooperation and assistance of the New York State Department of Transportation, Bureau of Soil Mechanics, the New York State Education Department, Museum and Science Service, and G. A. Connally of the State University of New York at New Paltz, during this study are gratefully acknowledged. Much of the preliminary field work was done by G. L. Giese and W. A. Hobba, Jr., U.S. Geological Survey, as part of a water-resources study of the Lake Champlain basin. The field work was supervised by R. C. Heath, former district chief of the Water Resources Division, U.S. Geological Survey. G. G. Parker, district chief, supervised the preparation of this report.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr67125","collaboration":"Prepared in cooperation with New York State Conservation Department","usgsCitation":"Kantrowitz, I., 1968, Ground-water resources in the vicinity of the Crown Point Fish Hatchery, Essex County, New York: U.S. Geological Survey Open-File Report 67-125, iii, 13 p., https://doi.org/10.3133/ofr67125.","productDescription":"iii, 13 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":177437,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr67125.jpg"},{"id":316602,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0125/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New York","county":"Essex County","otherGeospatial":"Crown Point Fish Hatchery","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.49990844726561,\n 43.92027700859655\n ],\n [\n -73.49990844726561,\n 43.95402351765834\n ],\n [\n -73.44677925109863,\n 43.95402351765834\n ],\n [\n -73.44677925109863,\n 43.92027700859655\n ],\n [\n -73.49990844726561,\n 43.92027700859655\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9fe4b07f02db660fc4","contributors":{"authors":[{"text":"Kantrowitz, I.H.","contributorId":15646,"corporation":false,"usgs":true,"family":"Kantrowitz","given":"I.H.","affiliations":[],"preferred":false,"id":245619,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47214,"text":"ofr68303 - 1968 - Geologic map of the 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}],"supersededBy":{"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"},"lastModifiedDate":"2022-04-27T18:07:21.153215","indexId":"ofr68303","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-303","title":"Geologic map of the east flank of the Elkhorn Mountains, Broadwater County, Montana","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68303","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1968, Geologic map of the east flank of the Elkhorn Mountains, Broadwater County, Montana: U.S. Geological Survey Open-File Report 68-303, 4 Plates: 22.11 x 82.09 inches or smaller, https://doi.org/10.3133/ofr68303.","productDescription":"4 Plates: 22.11 x 82.09 inches or smaller","costCenters":[],"links":[{"id":168100,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":399775,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0303/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":399774,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0303/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":399773,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0303/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":399772,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0303/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397076,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8295.htm"}],"scale":"24000","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 \"type\": \"Polygon\",\n \"coordinates\": [\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 -111.75,\n 46.125\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688b84","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":531710,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15262,"text":"ofr68206 - 1968 - Subsurface geology of the Silent Canyon caldera, Nevada Test Site, Nevada","interactions":[],"lastModifiedDate":"2025-06-20T18:13:29.768884","indexId":"ofr68206","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-206","title":"Subsurface geology of the Silent Canyon caldera, Nevada Test Site, Nevada","docAbstract":"Deep drilling in the vicinity of Silent Canyon on eastern Pahute Mesa, Nevada, has revealed a Tertiary volcanic section locally thicker than 14,000 feet. The area drilled covers most of the Silent Canyon caldera and some of the surrounding area. The caldera is rudely elliptical in plan and measures 10 by 14 miles.
Except on its east edge, the caldera is completely obscured by younger volcanic rocks, including ash-flow sheets from several other centers. The structure, originally inferred from surface mapping and a 20-mgal gravity low, has been confirmed by drilling at 21 sites.
Petrographic, chemical, and magnetic studies of more than 4,000 feet of drill core have revealed a complex sequence of volcanic rocks. Precaldera rocks include thick talc-alkalic lavas and tuffs. Peralkaline lavas and tuffs of the Silent Canyon center include the Belted Range Tuff (13-14 m.y.), eruption of which resulted in caldera collapse. The Belted Range Tuff has been downdropped 5,000-7,000 feet in the caldera. Subsequently, the depression was partially filled in the eastern part by genetically related peralkaline lavas and tuffs and in the western part by later calc -alkaline lavas and tuffs apparently genetically unrelated to the peralkaline rocks of the Silent Canyon center. Renewed subsidence probably occurred during their eruption.
Isopach maps of younger tuffs show that the caldera was topographically low during deposition of later (12.5-7 m.y.) ash-flow sheets from other volcanic centers.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68206","usgsCitation":"Orkild, P.P., Byers, F., Hoover, D.L., and Sargent, K.A., 1968, Subsurface geology of the Silent Canyon caldera, Nevada Test Site, Nevada: U.S. Geological Survey Open-File Report 68-206, 19 p., https://doi.org/10.3133/ofr68206.","productDescription":"19 p.","costCenters":[],"links":[{"id":491051,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0206/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147986,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0206/report-thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Silent Canyon","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"id\":\"37\",\"properties\":{\"name\":\"Nevada\",\"nation\":\"USA 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","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68134","usgsCitation":"Holmes, G.W., 1968, Preliminary materials map, Pittsfield East quadrangle, Massachusetts: U.S. Geological Survey Open-File Report 68-134, Report: 15 p.; 1 Plate: 26.82 × 28.79 inches, https://doi.org/10.3133/ofr68134.","productDescription":"Report: 15 p.; 1 Plate: 26.82 × 28.79 inches","costCenters":[],"links":[{"id":144674,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0134/report-thumb.jpg"},{"id":42838,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0134/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42839,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0134/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397581,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8257.htm"}],"scale":"24000","country":"United States","state":"Massachusetts","otherGeospatial":"Pittsfield East quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.25,\n 42.375\n ],\n [\n -73.125,\n 42.375\n ],\n [\n -73.125,\n 42.5\n ],\n [\n -73.25,\n 42.5\n ],\n [\n -73.25,\n 42.375\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66ce5b","contributors":{"authors":[{"text":"Holmes, George William","contributorId":79107,"corporation":false,"usgs":true,"family":"Holmes","given":"George","email":"","middleInitial":"William","affiliations":[],"preferred":false,"id":169032,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3073,"text":"wsp1830B - 1968 - Summary of floods in the United States during 1963","interactions":[],"lastModifiedDate":"2017-09-04T16:57:11","indexId":"wsp1830B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1830","chapter":"B","title":"Summary of floods in the United States during 1963","docAbstract":"This report describes the most outstanding floods in the United States during 1963. The three most destructive floods occurred in March from Alabama to West Virginia and Ohio, in June in Nebraska, and in August in Buffalo, N.Y.
Widespread disastrous floods struck the western slopes of the Appalachian Mountains from Alabama to West Virginia and Ohio as a result of three storms moving over the area during March 4-19. Precipitation during the first storm period, March 4-6, caused some major stream overflows and produced conditions favorable for high runoff from subsequent rainfall. Heavy rainfall on March 11-13 produced record-breaking floods on many streams in Tennessee, Kentucky, Virginia, and West Virginia. Noteworthy floods occurred in the bordering States of Alabama, Georgia, North Carolina, and Ohio. The third storm on If arch 16-19 was .significant because it prolonged the period of flooding and produced high-volume runoff in some areas. Twenty-six lives were lost, and more than 30,000 persons were forced from their homes. Damage to highways, railroads municipal and private property amounted to approximately \\$98 million.
Floods of June 24 in small basins in east-central Nebraska were the most severe known in the area. Discharges in many streams greatly exceeded the 50-year flood. Twenty-five cities and villages and more than 600 families suffered property loss. Three lives were lost. Property loss was about \\$13 million.
On July 29 the most severe rainstorm in 18 years occurred in western New York. On August 7, rains of near-record magnitude again fell over western New York, and record intensities were recorded in Buffalo for 1-, 2-, and 6-hour storms. The resulting floods on Scajaquada Creek were the highest recorded in a short period of record, and flood damage in Buffalo was estimated at \\$35 million.
In addition to the three floods mentioned above, 21 others of lesser magnitude are considered important enough to be included in this annual summary.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1830B","collaboration":"Prepared in cooperation with Federal, State, and local agencies","usgsCitation":"Rostvedt, J., and and others, 1968, Summary of floods in the United States during 1963: U.S. Geological Survey Water Supply Paper 1830, vi, 120 p., https://doi.org/10.3133/wsp1830B.","productDescription":"vi, 120 p.","numberOfPages":"130","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":29942,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1830b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139408,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1830b/report-thumb.jpg"}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db699262","contributors":{"authors":[{"text":"Rostvedt, J.O.","contributorId":24757,"corporation":false,"usgs":true,"family":"Rostvedt","given":"J.O.","email":"","affiliations":[],"preferred":false,"id":146242,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"and others","contributorId":127886,"corporation":true,"usgs":false,"organization":"and others","id":528057,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2341,"text":"wsp1854 - 1968 - Ground-water hydrology of the Sevier Desert, Utah","interactions":[],"lastModifiedDate":"2017-09-04T17:15:01","indexId":"wsp1854","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1854","title":"Ground-water hydrology of the Sevier Desert, Utah","docAbstract":"The Sevier Desert, as used in this report, comprises the main part of the Sevier Desert, the Tintic Valley, and the southeastern part of the Old River Bed. It covers an area of about 3,000 square miles and occupies a large basin in the eastern part of the Basin and Range physiographic province.
Large alluvial fans extend from the mountain fronts into the basin where they interfinger with eolian and lacustrine deposits and with fluvial deposits of the Sevier River. These unconsolidated deposits form a multiaquifer artesian system that is more than 1,000 feet thick and that extends from near the area of main recharge along the east side of the basin to Sevier Lake.
Most of the recharge to the ground-water reservoir results from water entering alluvial fans as percolation from streams, irrigation ditches, and irrigated fields. Another important source may be water in the limestone, quartzite, and other consolidated rocks in the mountains that border the basin. Leakage from the Central Utah Canal is a major source of recharge to the water-table aquifer.
Flowing wells are common in the central lowland part of the Sevier Desert, but as a result of below-normal precipitation and an increase in withdrawals from wells during 1950-64, the area of flowing wells has decreased. The quantity of ground water being wasted from flowing wells is not more than a few hundred acre-feet a year.
The amount of water discharged by withdrawal from wells has increased nearly 15 times since 1950 (from 2,000 acre-feet in 1950 to 30,000 acre-feet in 1964). As a result of this increasing withdrawal, the water levels in observation wells have declined 4 feet in areas of small withdrawals to more than 7 feet near centers of pumping for public supplies and irrigation.
An estimated 135,000-175,000 acre-feet of ground water is consumed by evapotranspiration each year in the 440,000 acres of desert that mainly support phreatophytes. This rate of discharge has changed little since 1950. The consumptive waste of ground water by undesirable phreatophytes, principally saltcedar and pickleweed, was not a serious problem in 1964 but could become a serious problem in the near future if saltcedar is permitted to spread.
Water levels in wells changed little during 1935-40. During 1941-50, however, water levels rose in response to the general above-normal precipitation during 1939-47. During 1950-64 water levels declined, partly in response to below-normal precipitation and partly in response to an increase in pumping from irrigation wells. Although the period 1961-63 was one of above-normal precipitation, water levels continued the overall decline that was started in 1950. The decline, therefore, probably is due to increased pumping.
The amount of water that could be obtained from storage if the piezometric surface in the artesian aquifer were lowered 20 feet is estimated to be 120,006 acre-feet. The specific capacities of wells used for irrigation and public supply range from 5 to 215 gallons per minute per foot of drawdown. Specific capacities generally decrease with increasing distances away from the edge of the basin.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1854","collaboration":"Prepared in cooperation with the Utah State Engineer","usgsCitation":"Mower, R.W., and Feltis, R., 1968, Ground-water hydrology of the Sevier Desert, Utah: U.S. Geological Survey Water Supply Paper 1854, Report: v, 75 p.; 7 Plates: 30.00 in. x 24.82 in. or smaller, https://doi.org/10.3133/wsp1854.","productDescription":"Report: v, 75 p.; 7 Plates: 30.00 in. x 24.82 in. or smaller","numberOfPages":"88","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":28244,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-7.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Sevier Desert, Utah, showing areas of phreatophyte growth in 1963"},{"id":138337,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1854/report-thumb.jpg"},{"id":28238,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Sevier Desert, Utah, showing location of selected wells and hydrogeochemical data"},{"id":28241,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-4.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Sevier Desert, Utah, showing average annual precipitation (1931-60) and recharge areas along the north and east edges"},{"id":28242,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-5.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Sevier Desert, Utah, showing areas of artesian flow during 1935 and March 1964 and water-level contours in the upper artesian and unconfined aquifers in March 1964"},{"id":28243,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-6.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map of the Sevier Desert, Utah, showing total dissolved solids in water from wells finished in the artesian aquifers, springs, and streams"},{"id":28239,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Generalized geologic map of the Sevier Desert and adjacent mountains, Utah"},{"id":28240,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1854/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Geologic section across the Sevier Desert, Utah, showing generalized stratigraphy and lithology and selected parts from an electrical log from an oil test"},{"id":28245,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1854/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","otherGeospatial":"Sevier Desert","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa9e4b07f02db6682c2","contributors":{"authors":[{"text":"Mower, R. W.","contributorId":34898,"corporation":false,"usgs":true,"family":"Mower","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":145048,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Feltis, R.D.","contributorId":93467,"corporation":false,"usgs":true,"family":"Feltis","given":"R.D.","affiliations":[],"preferred":false,"id":145049,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":19921,"text":"ofr68170 - 1968 - Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah","interactions":[{"subject":{"id":19921,"text":"ofr68170 - 1968 - Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah","indexId":"ofr68170","publicationYear":"1968","noYear":false,"title":"Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":6172,"text":"pp688 - 1971 - Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah","indexId":"pp688","publicationYear":"1971","noYear":false,"title":"Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah"},"id":1}],"supersededBy":{"id":6172,"text":"pp688 - 1971 - Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah","indexId":"pp688","publicationYear":"1971","noYear":false,"title":"Sedimentary features of the Blackhawk Formation (Cretaceous) in the Sunnyside District, Carbon County, Utah"},"lastModifiedDate":"2012-02-02T00:07:42","indexId":"ofr68170","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-170","title":"Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah","docAbstract":"The Blackhawk Formation at Sunnyside, Utah, was deposited along the western margin of the Western Interior Cretaceous sea during southeastward withdrawal of the sea. Sand was the dominant type of land-derived sediment deposited in the Sunnyside district during the regressive phases. Sand bodies prograded seaward in response to changing sediment supply from a source west of Sunnyside. Where conditions were favorable for the accumulation of vegetable material, peat deposits formed and were later changed to bituminous Coal by diagenesis. Studies of the coal bed show that the coals were formed from accumulation of small, low-growing plants and plant debris that was transported into the area of accumulation. Remains of large plants in the coals are rare. \r\n\r\nTrace fossils, which are tracks, trails and burrows formed by organisms and preserved in the rock, are extremely abundant in the Blackhawk rocks. These biogenic sedimentary structures are common in Cretaceous deposits throughout the western United States. Trace fossil distribution in the rocks is controlled by the depositional environment preferred by their creators. A study of the trace fossils of a. locality allows a more precise determination of the conditions during deposition of the sediments. Water depth, bottom conditions, salinity, current velocity and amount of suspended nutrients in the water are some of the environmental factors that may be reconstructed by studying trace fossils. \r\n\r\nThe Blackhawk Formation at Sunnyside comprises the members, the Kenilworth Member and the Sunnyside Member. Field studies show that the formation may be further subdivided in the Sunnyside district., according to the precepts of units of mappable thickness and similar lithologic characteristics. The Blackhawk pinches out eastward and north. ward into the Mancos Shale, and names for submembers become meaningless. Names are of value in the region of interest, however, because of the prominence of the named units. \r\n\r\nCoal mining is the main industry of the Book Cliffs region. Mines of the Sunnyside district are plagued by coal mine bumps, which are sudden, catastrophic releases of stress in the coal. Bumps cause loss of life, property age, and loss of profit to mining companies. Bumps occur when shear stress built up in the coal exceeds the shear Strength of the coal. Differential overburden pressure, faulting and tectonic activity, and lithology and structure of roof rocks are factors which influence bumps. Petroleum and natural gas (methane), which occur locally in pockets in the roof rocks above coal beds, may be diagenetic products of organic-rich sediments.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/ofr68170","usgsCitation":"Maberry, J.O., 1968, Sedimentary features of the Blackhawk formation (Cretaceous) at Sunnyside, Carbon County, Utah: U.S. Geological Survey Open-File Report 68-170, 180 p. ill., maps ;28 cm., https://doi.org/10.3133/ofr68170.","productDescription":"180 p. ill., maps ;28 cm.","costCenters":[],"links":[{"id":153250,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0170/report-thumb.jpg"},{"id":49428,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0170/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49429,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0170/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49430,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0170/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":49431,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0170/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbda6","contributors":{"authors":[{"text":"Maberry, John O.","contributorId":87134,"corporation":false,"usgs":true,"family":"Maberry","given":"John","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":181740,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15648,"text":"ofr68229 - 1968 - Geology and lode gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska","interactions":[{"subject":{"id":15648,"text":"ofr68229 - 1968 - Geology and lode gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska","indexId":"ofr68229","publicationYear":"1968","noYear":false,"title":"Geology and lode gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":39672,"text":"pp625B - 1970 - Geology and lode-gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska","indexId":"pp625B","publicationYear":"1970","noYear":false,"chapter":"B","title":"Geology and lode-gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska"},"id":1}],"supersededBy":{"id":39672,"text":"pp625B - 1970 - Geology and lode-gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska","indexId":"pp625B","publicationYear":"1970","noYear":false,"title":"Geology and lode-gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska"},"lastModifiedDate":"2023-07-24T20:55:05.501281","indexId":"ofr68229","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-229","title":"Geology and lode gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska","docAbstract":"Nuka Bay is a deep, T-shaped fiord on the southeast coast of the Kenai Peninsula approximately 60 miles southwest of the port of Seward. Gold-bearing quartz veins were discovered in the area in 1918, and between 1920 and 1940 several small mines were in operation around the North and West Arms of the bay. Estimated total production may have been as much as $164,000.
Bedrock in the Nuka Bay area is a thick Cretaceous section of interbedded slate and graywacke that has been regionally deformed into a series of relatively open, but overturned, folds plunging at low angler to the north-northeast. Except at the folds, bedding and foliation (slaty cleavage) are parallel and dip steeply to the northwest. Small granodiorite dikes fill tensional cross joints in the folded sediments, and a few granodiorite sills are intruded along bedding and foliation planes.
Quartz veins are abundant throughout the region, but contain significant amounts of gold only in a relatively small area, 8 miles long and 6 miles wide, around North and West Arms. The veins are generally less than 5 feet wide and 300 feet long and consist chiefly of massive white quartz. Arsenopyrite with minor amounts of other sulfide and native gold occurs as irregular masses and pods in the quartz. The larger and more productive veins dip steeply and strike east-west, almost normal to the regional structure, and appear to be confined to competent graywacke beds or dikes. Random channel sampling of the quartz veins indicates gold values as high as 9 ounces per ton across zones as wide as 2 feet.
A study of the stream sediments throughout the area disclosed several drainages with detectable gold; one, Babcock Creek, contained 0.5 ppm gold, the others from 0.02 to 0.07 ppm. No base metal anomalies were detected. The area appears to warrant further investigation as a potential producer of small amounts of gold. Diligent smell-scale mining may be economically feasible.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68229","usgsCitation":"Richter, D.H., 1968, Geology and lode gold deposits of the Nuka Bay area, Kenai Peninsula, Alaska: U.S. Geological Survey Open-File Report 68-229, iv, 52 p., https://doi.org/10.3133/ofr68229.","productDescription":"iv, 52 p.","costCenters":[],"links":[{"id":419268,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0229/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146904,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0229/report-thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Kenai Peninsula, Nuka Bay area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -150.66230433486226,\n 59.562476930416636\n ],\n [\n -150.66230433486226,\n 59.302789270633326\n ],\n [\n -150.29991099261446,\n 59.302789270633326\n ],\n [\n -150.29991099261446,\n 59.562476930416636\n ],\n [\n -150.66230433486226,\n 59.562476930416636\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db685281","contributors":{"authors":[{"text":"Richter, Donald H.","contributorId":61021,"corporation":false,"usgs":true,"family":"Richter","given":"Donald","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":171491,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2589,"text":"wsp1852 - 1968 - Water resources of King County, Washington","interactions":[],"lastModifiedDate":"2023-01-03T21:32:56.352719","indexId":"wsp1852","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"1852","title":"Water resources of King County, Washington","docAbstract":"Although the total supply of water in King County is large, water problems are inevitable because of the large and rapidly expanding population. The county contains a third of the 3 million people in Washington, most of the population being concentrated in the Seattle metropolitan area.
King County includes parts of two major physiographic features: the western area is part of the Puget Sound Lowland, and the eastern area is part of the Cascade Range. In these two areas, the terrain, weather, and natural resources (including water) contrast markedly.
Average annual precipitation in the county is about 80 inches, ranging from about 30 inches near Puget Sound to more than 150 inches in parts of the Cascades. Annual evapotranspiration is estimated to range from 15 to 24 inches.
Average annual runoff ranges from about 15 inches in the lowlands to more than 100 inches in the mountains. Most of the streamflow is in the major basins of the county--the Green-Duwamish, Lake Washington, and Snoqualmie basins. The largest of these is the Snoqualmie River basin (693 square miles), where average annual runoff during the period 1931-60 was about 79 inches. During the same period, annual runoff in the Lake Washington basin ( 607 square miles) averaged about 32 inches, and in the Green-Duwamish River basin (483 square miles), about 46 inches. Seasonal runoff is generally characterized by several high-flow periods in the winter, medium flows in the spring, and sustained low flows in the summer and fall.
When floods occur in the county they come almost exclusively between October and March. The threat of flood damage is greatest on the flood plaits of the larger rivers, but in the Green-Duwamish Valley the threat was greatly reduced with the completion of Howard A. Hanson Dam in 1962. In the Snoqualmie River basin, where no such dam exists, the potential damage from a major flood increases each year as additional land is developed in the Snoqualmie Valley.
Only moderate amounts of sediment are transported by most streams in the county, except during short periods of heavy rain in the winter. The temperature and chemical quality of surface waters are well suited to the requirements of fisheries and for municipal, industrial, and domestic supplies. Little treatment is needed for most uses of surface water, except where the water is subject to pollution.
Most recoverable ground water in the county occurs in the Puget Sound Lowland, where great volumes of unconsolidated sedimentary deposits were left by the continental glaciers of the Pleistocene Epoch. Bedrock, most of which is in the Cascade Range, contains very little ground water. Numerous springs, largely undeveloped, occur in several parts of the county.
Most of the ground water is of good to excellent quality except for excessive iron, which in some places may require treatment of the water before it is suitable for domestic or industrial use.
Excluding water used for hydroelectric-power, recreation, and fisheries, more than 80 percent of the water used in the county is provided by municipal-supply systems. Each of the major river basins includes municipal watersheds that provide large supplies of excellent water. By the 1980's, more than 90 percent of the county's population will probably be served by the Seattle municipal supply. With full development, Seattle's water system would have a capacity sufficient to supply more than 2 million people with 300 gallons per person per day. Most industrial and commercial establishments in the county obtain water from public supply systems.
The most serious water problem in the county at present (1965) is the threat of pollution in the densely populated areas. The immediate threat in the Seattle area is being reduced by the sewage-treatment program of the Municipality of Metropolitan Seattle, which will eliminate the discharge of waste into Lake Washington. Expected increases in population and industry will introduce new problems that will require additional planning to assure adequate water quality for fisheries, recreation, and other uses.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1852","usgsCitation":"Richardson, D., Bingham, J., Madison, R.J., and Williams, R., 1968, Water resources of King County, Washington: U.S. Geological Survey Water Supply Paper 1852, Report: v, 74 p.; 2 Plates: 20.00 x 22.80 inches and 20.00 x 19.24 inches, https://doi.org/10.3133/wsp1852.","productDescription":"Report: v, 74 p.; 2 Plates: 20.00 x 22.80 inches and 20.00 x 19.24 inches","costCenters":[],"links":[{"id":411295,"rank":5,"type":{"id":36,"text":"NGMDB Index 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J.","contributorId":84734,"corporation":false,"usgs":true,"family":"Madison","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145453,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Williams, R.","contributorId":7686,"corporation":false,"usgs":true,"family":"Williams","given":"R.","affiliations":[],"preferred":false,"id":145450,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":32657,"text":"pp516E - 1968 - A geophysical study in Grand Teton National Park and vicinity, Teton County, Wyoming","interactions":[],"lastModifiedDate":"2025-05-21T17:47:12.819568","indexId":"pp516E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"516","chapter":"E","title":"A geophysical study in Grand Teton National Park and vicinity, Teton County, Wyoming","docAbstract":"An integrated geophysical study - comprising gravity, seismic refraction, and aeromagnetic surveys - was made of a 4,600-km2 area in Grand Teton National Park and vicinity, Wyoming, for the purpose of obtaining a better understanding of the structural relationships in the region. The Teton range is largely comprised of Precambrian crystalline rocks and layered metasedimentary gneiss, but it also includes granitic gneiss, hornblende-plagioclase gneiss, granodiorite, and pegmatite and diabase dikes. Elsewhere, the sedimentary section is thick. The presence of each system except Silurian provides a chronological history of most structures. Uplift of the Teton-Gros Ventre area began in the Late Cretaceous; most of the uplift occurred after middle Eocene time. Additional uplift of the Teton Range and downfaulting of Jackson Hole began in the late Pliocene and continues to the present.
Bouguer anomalies range from -185 mgal over Precambrian rocks of the Teton Range to -240 mgal over low-density Tertiary and Cretaceous sedimentary rocks of Jackson Hole. The Teton fault (at the west edge of Jackson Hole), as shown by steep gravity gradients and seismic-refraction data, trends north-northeast away from the front of the Teton Range in the area of Jackson Lake. The Teton fault either is shallowly inclined in the Jenny Lake area, or it consists of a series of fault steps in the fault zone; it is approximately vertical in the Arizona Creek area.
Seismic-refraction data can be fitted well by a three-layer gravity model with velocities of 2.45 km per sec for the Tertiary and Cretaceous rocks above the Cloverly Formation, 3.9 km per sec for the lower Mesozoic rocks, and 6.1 km per sec for the Paleozoic (limestone and dolomite) and Precambrian rocks. Gravity models computed along two seismic profiles are in good agreement (σ=± 2 mgal) if density contrasts with the assumed 2.67 g per cm3 Paleozoic and Precambrian rocks are assumed to be -0.35 and -0.10 g per cm3 for the 2.45 and 3.9 km per sec velocity layers, respectively. The Teton Range has a maximum vertical uplift of about 7 km, as inferred from the maximum depth to basement of about 5 km.
Aeromagnetic data show a 400γ positive anomaly in the Gros Ventre Range, which trends out of the surveyed area at the east edge. Exposed Precambrian rocks contain concentrations of magnetite and hematite. A prominent anomaly of about 100γ is associated with the Gros Ventre Range, and 100γ anomalies are associated with the layered gneiss of the Teton Range. On this basis the unmapped Precambrian rocks of the Gross Ventre Range are interpreted as layered gneiss. The sources of the magnetic anomalies, as indicated by depth determination, are at the surface of the Precambrian rocks. A model fitted to a profile across the Gros Ventre Range gives a depth to the Precambrian surface and a susceptibility of 0.0004 emu (electromagnetic units) for the source, which is consistent with modal analyses of the layered gneisses. A residual magnetic map shows that the granitic rocks and layered gneiss probably continue beneath the floor of Jackson Hole east of the Teton fault. The location of aeromagnetic anomalies is consistent with the interpretation that the Teton fault diverges from the front of the Teton Range.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Geophysical field investigations, 1964-67 (Professional Paper 516)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp516E","usgsCitation":"Behrendt, J.C., Tibbetts, B.L., Bonini, W.E., Lavin, P.M., Love, J.D., and Reed, J., 1968, A geophysical study in Grand Teton National Park and vicinity, Teton County, Wyoming: U.S. Geological Survey Professional Paper 516, Report: v, 23 p.; 3 Plates: 14.00 × 20.00 inches or smaller, https://doi.org/10.3133/pp516E.","productDescription":"Report: v, 23 p.; 3 Plates: 14.00 × 20.00 inches or smaller","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":125352,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0516e/report-thumb.jpg"},{"id":60549,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0516e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":394917,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4545.htm"},{"id":60546,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0516e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60547,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0516e/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":60548,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0516e/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Wyoming","county":"Teton County","otherGeospatial":"Grand Teton National Park and vicinity","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.0223388671875,\n 43.09697190802465\n ],\n [\n -110.2313232421875,\n 43.09697190802465\n ],\n [\n -110.2313232421875,\n 44.15068115978094\n ],\n [\n -111.0223388671875,\n 44.15068115978094\n ],\n [\n -111.0223388671875,\n 43.09697190802465\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd4957e4b0b290850ef129","contributors":{"authors":[{"text":"Behrendt, John Charles jbehrendt@usgs.gov","contributorId":74747,"corporation":false,"usgs":true,"family":"Behrendt","given":"John","email":"jbehrendt@usgs.gov","middleInitial":"Charles","affiliations":[],"preferred":false,"id":208873,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tibbetts, Benton L.","contributorId":105169,"corporation":false,"usgs":true,"family":"Tibbetts","given":"Benton","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":208875,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bonini, William E.","contributorId":87417,"corporation":false,"usgs":true,"family":"Bonini","given":"William","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":208874,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Lavin, Peter M.","contributorId":42087,"corporation":false,"usgs":true,"family":"Lavin","given":"Peter","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":208871,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Love, J. D.","contributorId":64620,"corporation":false,"usgs":true,"family":"Love","given":"J.","middleInitial":"D.","affiliations":[],"preferred":false,"id":208872,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Reed, John C. jreed@usgs.gov","contributorId":1259,"corporation":false,"usgs":true,"family":"Reed","given":"John C.","email":"jreed@usgs.gov","affiliations":[],"preferred":true,"id":208870,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":16445,"text":"ofr68315 - 1968 - Surface seismic measurements of the Project GASBUGGY explosion at intermediate distance ranges","interactions":[],"lastModifiedDate":"2012-08-01T01:01:41","indexId":"ofr68315","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1968","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":"68-315","title":"Surface seismic measurements of the Project GASBUGGY explosion at intermediate distance ranges","docAbstract":"Project GASBUGGY was an experiment performed by the Atomic Energy Commission, the El Paso Natural Gas Company, and the Bureau of Mines, U.S. Department of the Interior, to determine the effectiveness of a method for increasing the recovery of natural gas by large-scale fracturing of a gas-bearing formation with an underground nuclear explosion. The Project GASBUGGY nuclear explosive of 26 kilotons design yield was detonated on Sunday, December 10, 1967, at 1230:00 Mountain Standard Time. Lawrence Radiation Laboratory reported that the explosive was emplaced at 4240 ft below the ground surface, 1770 ft from the west line and 1218 ft from the south line in Section 36 of Township 29 North, Range 4 West, in Rio Arriba County, New Mexico, about 55 air miles east of the city of Farmington, New Mexico. The geodetic coordinates are: Latitude 36?40'40.4\" North, and Longitude 107?12'30.3\" West. The elevation of surface ground zero was 7204 ft above Mean Sea Level. The detonation occurred in the Lewis shale about 40 ft below its contact with the gas-bearing Pictured Cliffs sandstone. Early indications are that the explosive performed satisfactorily. This document is submitted as a preliminary data report. Additional analyses of the data will be prepared at a later time.","language":"ENGLISH","publisher":"National Center for Earthquake Research","publisherLocation":"Menlo Park, CA","doi":"10.3133/ofr68315","usgsCitation":"Warren, D.H., and Jackson, W.H., 1968, Surface seismic measurements of the Project GASBUGGY explosion at intermediate distance ranges: U.S. Geological Survey Open-File Report 68-315, 45 p. ill., maps ;27 cm., https://doi.org/10.3133/ofr68315.","productDescription":"45 p. ill., maps ;27 cm.","numberOfPages":"51","onlineOnly":"Y","additionalOnlineFiles":"N","costCenters":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"links":[{"id":148567,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_68_315.gif"},{"id":259292,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/0315/of68-315.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":259291,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/1968/0315/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"New Mexico","county":"Rio Arriba County","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b00e4b07f02db69824f","contributors":{"authors":[{"text":"Warren, David H.","contributorId":106128,"corporation":false,"usgs":true,"family":"Warren","given":"David","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":172863,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jackson, W. H.","contributorId":21153,"corporation":false,"usgs":true,"family":"Jackson","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":172862,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70114619,"text":"70114619 - 1968 - Ground-water resources of Monmouth County, New Jersey","interactions":[],"lastModifiedDate":"2015-10-17T19:43:54","indexId":"70114619","displayToPublicDate":"1970-01-01T11:02:47","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":126,"text":"New Jersey Division of Water Policy and Supply Special Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"23","title":"Ground-water resources of Monmouth County, New Jersey","docAbstract":"Monmouth County includes an area of 538 square miles in east-central New Jersey. The climate is characterized by moderate temperature, moderate humidity, and moderate precipitation.
\nThe exposed rocks in the area are chiefly sands and clays, which range in age from Late Cretaceous through Recent. The formations strike northeast-southwest and dip gently to the southeast. These rocks range in total thickness from about 500 to 1,200 feet or more and are underlain by basement rocks of late Precambrian (?) age.
\nThe principal aquifers underlying Monmouth County occur in the Raritan and Magothy Formations, the Englishtown Formation, the Wenonah Formation and Mount Laurel Sand, the Vincentown Formation, and the Kirkwood Formation.
\nGround water constituted about 50 percent of the total water use in 1958. The daily withdrawal of ground water was at an average rate of 21.6 mgd (million gallons per day) in 1958 and about 32 mgd in 1965 (N. J. Division of Water Policy and Supply). The water demand is expected to increase to about 133 mgd by the year 2000. An analysis of streamflow records for the period 1932 to 1950 suggests that, excluding the Raritan and Magothy Formations, the major aquifers that occur under water-table conditions in the county discharge an average of about 178 mgd to streams.
\nThe aquifers in the Raritan and Magothy Formations contribute little or no water directly to streams in Monmouth County. These aquifers have been the most productive in the county. However, because salt water has been found in the lower parts of these formations in Ocean County, further development should proceed watchfully to assure that salt water does not threaten existing supplies.
\nAquifers in the Raritan and Magothy Formations and the Englishtown Formation supplied 76 percent of the ground water used in 1958. These aquifers, in conjunction with the Wenonah Formation and Mount Laurel Sand of Late Cretaceous age, are capable of providing relatively large yields to wells. The average yield of 63 large-diameter wells tapping these aquifers is 580 gpm, at depths randing from 100 to 1,140 feet. In general, the concentrations of chemical constituents in water from the aquifers would not restrict the use of the water for most purposes. High concentrations of iron do occur and require treatment. The concentrations of dissolved solids in 39 to 41 samples were 160 ppm (parts per million) or less.
","language":"English","publisher":"New Jersey Department of Conservation and Economic Development, Division of Water Policy and Supply","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the State of New Jersey, Department of Conservation and Economic Development, Division of Water Policy and Supply","usgsCitation":"Jablonski, L.A., 1968, Ground-water resources of Monmouth County, New Jersey: New Jersey Division of Water Policy and Supply Special Report 23, ix, 117 p.","productDescription":"ix, 117 p.","numberOfPages":"130","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":290150,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":290149,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70114619/report.pdf"}],"country":"United States","state":"New Jersey","county":"Monmouth County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -74.613529,40.07913 ], [ -74.613529,40.478576 ], [ -73.972184,40.478576 ], [ -73.972184,40.07913 ], [ -74.613529,40.07913 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ad40f2e4b0729c154181cc","contributors":{"authors":[{"text":"Jablonski, Leo A.","contributorId":16324,"corporation":false,"usgs":true,"family":"Jablonski","given":"Leo","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":495355,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207397,"text":"70207397 - 1968 - The age of the Puerto Rico Trench","interactions":[],"lastModifiedDate":"2019-12-19T14:04:13","indexId":"70207397","displayToPublicDate":"1968-12-31T15:08:58","publicationYear":"1968","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}},"title":"The age of the Puerto Rico Trench","docAbstract":"The Puerto Rico Trench is parallel to and north of Puerto Rico and the Virgin Islands and reaches depths of more than 8000 meters. Puerto Rico, the closest land area, has a central longitudinal core of Cretaceous and early Tertiary volcanic rocks, some serpentinite of undetermined age, and numerous small intrusions. These rocks were folded into an anticlinorium and intensely faulted into hundreds of fault blocks in an orogeny that lasted from Late Cretaceous until middle Eocene time. Most fold axes and the major fault zones trend approximately west-northwest at an angle of about 15° to the general trend of the island and to the Puerto Rico Trench. Near the north coast, late Oligocene rocks rest on a truncated surface of Cretaceous and early Tertiary volcanic rocks. The Oligocene and overlying Miocene sedimentary rocks strike approximately east, parallel to the Puerto Rico Trench. Apparently the trench is not related to the tectonic movements that folded and faulted the Cretaceous and early Tertiary rocks, but it is closely related tectonically to the Oligocene and Miocene rocks. The trench probably first appeared in Oligocene or possibly late Eocene time and may have reached its maximum depth in late Miocene or Pliocene time.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[487:TAOTPR]2.0.CO;2","issn":"00167606","usgsCitation":"Monroe, W.H., 1968, The age of the Puerto Rico Trench: Geological Society of America Bulletin, v. 79, no. 4, p. 487-494, https://doi.org/10.1130/0016-7606(1968)79[487:TAOTPR]2.0.CO;2.","productDescription":"8 p. 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Predators were removed from the west side of the Refuge while the east side served as a control area. At the end of 3 years, these areas were reversed to reduce the effects of environmental influences. The effect of predator removal was measured by a simulated nest study to determine predation pressure, a check of natural nest success, and weekly breeding pair and brood counts. Results indicated that 60 percent more Class I ducklings were produced on the units where predator control was conducted. Until more is known, reduction of predators to increase waterfowl nesting success should be limited to intensively managed production areas where substantial nest losses are demonstrated.","language":"English","publisher":"Wiley","doi":"10.2307/3799541","usgsCitation":"Balser, D.S., Dill, H.H., and Nelson, H., 1968, Effect of predator reduction on waterfowl nesting success: Journal of Wildlife Management, v. 32, no. 4, p. 669-682, https://doi.org/10.2307/3799541.","productDescription":"14 p.","startPage":"669","endPage":"682","costCenters":[],"links":[{"id":133748,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.er.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Minnesota","otherGeospatial":"Agassiz National Wildlife Refuge","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -96.08062071899535,\n 48.441308663632356\n ],\n [\n -96.08062071899535,\n 48.20707610545438\n ],\n [\n -95.76928748057993,\n 48.20707610545438\n ],\n [\n -95.76928748057993,\n 48.441308663632356\n ],\n [\n -96.08062071899535,\n 48.441308663632356\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"32","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db625327","contributors":{"authors":[{"text":"Balser, D. S.","contributorId":79436,"corporation":false,"usgs":true,"family":"Balser","given":"D.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":311842,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dill, Herbert H.","contributorId":40547,"corporation":false,"usgs":true,"family":"Dill","given":"Herbert","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":311841,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nelson, H.K.","contributorId":21489,"corporation":false,"usgs":true,"family":"Nelson","given":"H.K.","email":"","affiliations":[],"preferred":false,"id":311840,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70209020,"text":"70209020 - 1968 - Hornblendes from granitic rocks of the central Sierra Nevada batholith, California","interactions":[],"lastModifiedDate":"2021-08-26T13:47:25.051632","indexId":"70209020","displayToPublicDate":"1968-10-01T17:40:39","publicationYear":"1968","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":"Hornblendes from granitic rocks of the central Sierra Nevada batholith, California","docAbstract":"Twenty samples of hornblendes from rocks of 14 plutonic units in the central Sierra Nevada and Inyo Mountains, California, have been studied in detail. Optical, density, single-crystal and powder X-ray diffraction, and major and minor element chemical data are reported.The compositions of the hornblendes show only limited correlation with the chemistry of the rocks in which they occurred. Hornblendes from granitic rocks of the eastern Sierra Nevada and Inyo Mountains have a wide range of tetrahedral aluminum content which is often as low as three-quarters of an atom per formula unit, whereas hornblendes from younger granitic rocks elsewhere in the Sierra Nevada batholith contain more than one atom of tetrahedral aluminum per formula unit. Because an increase of aluminum in tetrahedral co-ordination is considered indicative of higher temperatures of crystallization, the observed differences in the hornblendes suggest that older plutonic rocks of the batholith may have been metamorphosed regionally or may have been affected by widespread hydrothermal action prior to consolidation of later granitic rocks.
","language":"English","publisher":"Oxford University Press","doi":"10.1093/petrology/9.3.378","usgsCitation":"Dodge, F.C., Papike, J.J., and Mays, R.E., 1968, Hornblendes from granitic rocks of the central Sierra Nevada batholith, California: Journal of Petrology, v. 9, no. 3, p. 378-410, https://doi.org/10.1093/petrology/9.3.378.","productDescription":"33 p.","startPage":"378","endPage":"410","costCenters":[],"links":[{"id":373142,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Central Sierra Nevada Batholith","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -120.08605957031249,\n 36.28413532741724\n ],\n [\n -117.80639648437499,\n 36.28413532741724\n ],\n [\n -117.80639648437499,\n 37.75768707689704\n ],\n [\n -120.08605957031249,\n 37.75768707689704\n ],\n [\n -120.08605957031249,\n 36.28413532741724\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"9","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Dodge, F. C. W.","contributorId":18755,"corporation":false,"usgs":true,"family":"Dodge","given":"F.","email":"","middleInitial":"C. W.","affiliations":[],"preferred":false,"id":784561,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Papike, J. J.","contributorId":18488,"corporation":false,"usgs":true,"family":"Papike","given":"J.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":784562,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mays, R. E.","contributorId":52722,"corporation":false,"usgs":true,"family":"Mays","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":784563,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70226796,"text":"70226796 - 1968 - Television observations from Surveyor 3","interactions":[],"lastModifiedDate":"2021-12-13T20:41:21.912777","indexId":"70226796","displayToPublicDate":"1968-06-15T14:33:18","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2312,"text":"Journal of Geophysical Research","active":true,"publicationSubtype":{"id":10}},"title":"Television observations from Surveyor 3","docAbstract":"A total of 6315 pictures were taken by the television camera on Surveyor 3 after the lunar landing. These pictures have provided much new information about the location of the landing site on the moon, the detailed topographic and geologic characteristics of the lunar surface, and the appearance of the earth as seen from the moon, both during eclipse of the sun and during partial direct illumination by the sun. Surveyor 3 landed in a subdued crater slightly more than 200 meters in diameter, which has a low rounded rim and is about 15 meters deep. The spacecraft is situated on the east wall of the crater, about half way between the center of the crater and the rim crest. The spacecraft is inclined 14.7° ± 1.0° toward the west. The selenographic coordinates of the landing site are 2.94°S latitude, 23.34°W longitude, relative to selenodetic control adopted by the Aeronautical Chart and Information Center.
Small morphologic elements of the landing site include small craters, linear ridges and troughs, and fragmental debris. The craters and fragmental debris resemble those observed at the Surveyor 1 landing site, both in distribution of shape and in distribution of size. Most of the craters in Surveyor 1 and 3 pictures are inferred to be of impact origin. Their size-frequency distribution corresponds to the distribution that would be produced by repetitive bombardment by meteoroids, a bombardment sufficiently prolonged that the crater population has reached a steady state or has come to equilibrium. Some of the craters observed at the Surveyor 3 landing site are inferred to be of secondary impact origin, and some probably have been formed either by subsidence or by drainage of fragmental debris into cracks or fissures in the subsurface. Fragmental debris at the landing site is inferred to have been derived primarily by the same process of repetitive bombardment that produced the majority of craters. The inferred volumetric size-frequency distribution of fragments, derived from the observed size distribution of fragments on the surface, is similar to the distribution that would be produced by repetitive bombardment of coherent rocks by meteoroids with a mass-frequency distribution like that found from observed meteors and recovered meteorites on earth. Two prominent strewn fields of blocky debris were observed around two craters, 13 and 15 meters across, at the Surveyor 3 site. The 13-meter crater has a sharp raised rim, and the 15-meter crater has a more subdued rounded rim. The blocks associated with the subdued crater have twice as high a mean roundness as the blocks associated with the raised-rim crater, and they are much more deeply buried. The size-frequency distribution function for the fragments in each of the strewn fields of blocks resembles the size-frequency distribution for fragments ejected by impacts in strong rock, such as Meteor Crater, Arizona. Most of the fragments at the surface of the Surveyor 3 landing site are evidently part of a layer of fragmental material of low cohesion that is at least 1 meter thick along the upper parts of the wall of the crater in which Surveyor 3 landed and may be much thicker near the center of the crater. The evidence from the Surveyor 3 pictures suggests that this layer of debris, or regolith, is subject to downslope creep or mass movement. Creep is probably caused by seismic shaking, due mainly to near and far impact events and perhaps due partly to internal lunar seismicity.
Disturbances of the lunar surface produced by Surveyor 3, like those produced by Surveyor 1, exposed material at depths of a few centimeters or less that was darker than the material at the surface. The albedo of the fine-grained fragmental debris is probably 20 to 30% lower at depths of only a fraction of a millimeter than it is at the optically observed surface. All coarse fragments protruding above the general level of the surface have a higher albedo than the fine-grained matrix of the surface. These general photometric relationships can be explained if it is assumed that the surfaces of the particles in the shallow lunar subsurface tend to become coated with a dark substance; the term proposed for this hypothetical substance is ‘lunar varnish’ On the protruding surface of blocks and coarse fragments the lunar varnish is scrubbed off by the processes that cause rounding. The exposed surfaces of fine particles on the lunar surface are similarly affected, but, because they are mixed relatively rapidly with particles just beneath the surface, the process is incomplete and the fine-grained material exposed at the lunar surface, therefore, has a lower albedo than blocks and other large fragments. Coating of particles by lunar varnish evidently takes place just beneath the surface. The estimated normal luminance factor (normal albedo) of an undisturbed part of the lunar surface next to footpad 2 of the Surveyor 3 spacecraft is 8.5%. An area of the lunar surface disturbed by the surface sampler has an estimated normal luminance factor of 6.6%, and fine-grained material placed on footpad 2 by the surface sampler has an estimated normal luminance factor of 7.6%. The errors in all these estimates may be as high as 25% because of uncertainties of correction required for light scattered from the camera mirror. Preliminary search for color differences, by color reconstitution methods, revealed no determinable differences in color among various coarse blocks, the fine-grained matrix of the surface, or fine-grained material disturbed by the surface sampler.
Surveyor 3 pictures of the eclipse of the sun by the earth revealed a bright region in the refraction halo surrounding the earth, which was correlated with the position of the sun, and a series of bright beads that occurred over regions of the earth largely clear of clouds. Clouds tend to occult the refracted rays of the sun, most of which pass through the lower part of the atmosphere at the limb; the beads occurred in the depressions in the optical silhouette of the earth. Preliminary reduction of the color of the refracted light showed that the brightest region, near the position of the sun, exhibited a correlated color temperature close to 4800°K. The color temperature tended to be lower for light that followed paths of greater atmospheric absorption. Preliminary analysis of Surveyor 3 pictures of the partly illuminated earth revealed colors similar to the colors recorded from orbit by the Mercury and Gemini astronauts.
","language":"English","publisher":"Wiley-Blackwell","doi":"10.1029/JB073i012p03989","usgsCitation":"Shoemaker, E.M., Batson, R.M., Holt, H.E., Morris, E.C., Rennilson, J.J., and Whitaker, E.A., 1968, Television observations from Surveyor 3: Journal of Geophysical Research, v. 73, no. 12, p. 3989-4043, https://doi.org/10.1029/JB073i012p03989.","productDescription":"55 p.","startPage":"3989","endPage":"4043","costCenters":[],"links":[{"id":392820,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Moon","volume":"73","issue":"12","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","contributors":{"authors":[{"text":"Shoemaker, Eugene Merle","contributorId":20342,"corporation":false,"usgs":true,"family":"Shoemaker","given":"Eugene","email":"","middleInitial":"Merle","affiliations":[],"preferred":false,"id":828303,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Batson, R. M.","contributorId":76714,"corporation":false,"usgs":true,"family":"Batson","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":828304,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Holt, H. E.","contributorId":64694,"corporation":false,"usgs":true,"family":"Holt","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":828305,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Morris, E. C.","contributorId":84381,"corporation":false,"usgs":true,"family":"Morris","given":"E.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":828306,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Rennilson, J. J.","contributorId":107336,"corporation":false,"usgs":true,"family":"Rennilson","given":"J.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":828307,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Whitaker, E. A.","contributorId":43086,"corporation":false,"usgs":true,"family":"Whitaker","given":"E.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":828308,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":70209035,"text":"70209035 - 1968 - Tectonic emplacement of the Burro Mountain ultramafic body, Santa Lucia Range, California","interactions":[],"lastModifiedDate":"2020-03-11T19:06:20","indexId":"70209035","displayToPublicDate":"1968-05-01T18:58:17","publicationYear":"1968","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":"Tectonic emplacement of the Burro Mountain ultramafic body, Santa Lucia Range, California","docAbstract":"The Burro Mountain body is a crudely equidimensional block of unusually fresh ultramafic rock. This block, along with numerous smaller and more elongate serpentinite bodies, has been emplaced in a highly sheared Franciscan terrane immediately west of the Nacimiento fault. This fault separates two major structural units: (1) on the east, a 40- by 300-mile block with basement of granitic rock, schists and gneisses, and (2) on the west, a 10- by 100-mile tract of Franciscan Formation.
Within the Burro Mountain body the primary rock types and their approximate percentages are: peridotite (65), dunite (35), and pseudopyroxenite (<1). Variations among these lithologic types produce a well-defined internal structure, the two major elements of which are: (1) pervasive compositional layering whose attitude throughout the body varies little from N. 5° W., 80° E., and (2) superimposed discordant structures which may cut the earlier layering at any angle. The first set is thought to have been formed by metamorphic differentiation associated with internal deformation, the second set by metasomatic replacement, possibly a succeeding phase of the earlier metamorphic differentiation.
Serpentinization is nearly complete at the margins but progressively decreases toward the center of the body. Contact metasomatism, related to Serpentinization, is responsible for the sporadic presence of rodingites around the margins. An arm-like extension of the main body and linear trains of serpentinite bodies extending for miles parallel to the regional structure may represent previous marginal material sheared out during emplacement. The tectonic nature of the emplacement is demonstrated by the discordance of internal versus regional structure, discrepancy of metamorphic grade between ultramafic and country rock, extreme marginal shearing, lack of igneous contacts, and association with other tectonic inclusions.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[527:TEOTBM]2.0.CO;2","usgsCitation":"Burch, S.H., 1968, Tectonic emplacement of the Burro Mountain ultramafic body, Santa Lucia Range, California: GSA Bulletin, v. 79, no. 5, p. 527-544, https://doi.org/10.1130/0016-7606(1968)79[527:TEOTBM]2.0.CO;2.","productDescription":"18 p.","startPage":"527","endPage":"544","costCenters":[],"links":[{"id":373156,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Burro Mountain, Santa Lucia Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.30313873291016,\n 35.83743752447774\n ],\n [\n -121.24048233032227,\n 35.83743752447774\n ],\n [\n -121.24048233032227,\n 35.88571227867025\n ],\n [\n -121.30313873291016,\n 35.88571227867025\n ],\n [\n -121.30313873291016,\n 35.83743752447774\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"79","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Burch, Stephen H.","contributorId":19150,"corporation":false,"usgs":true,"family":"Burch","given":"Stephen","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":784596,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221378,"text":"70221378 - 1968 - New theory of recharge to the artesian basin of the Dakotas","interactions":[],"lastModifiedDate":"2021-06-11T17:40:06.499376","indexId":"70221378","displayToPublicDate":"1968-02-01T12:34:38","publicationYear":"1968","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}},"title":"New theory of recharge to the artesian basin of the Dakotas","docAbstract":"The artesian basin of the Dakotas has been studied for many years. The widely held concept has been that recharge enters the equivalents of the Dakota Sandstone, where they are exposed on the flanks of the Black Hills, and moves through this formation to the area of maximum development of the aquifer in eastern North Dakota and South Dakota. Some anomalies, difficult to explain by this concept, have remained unresolved. According to the theory here proposed, recharge enters the Lower Mississippian Pahasapa Limestone and the underlying Englewood Formation where they are exposed on the flanks of the Black Hills. The Pahasapa is in part the equivalent of the Lower and Upper Mississippian Madison Group. The limestones are very cavernous where exposed on the flanks of the Black Hills, and seemingly in the subsurface as well. Streams flowing east from the Precambrian core of the Hills lose virtually all their flow in crossing the cavernous limestones. Widespread karst topography was developed on the Madison during the erosion period which preceded deposition of the Pennsylvanian and Permian Minnelusa Formation. Water moves freely through the cavernous limestone with little head loss for more than 100 miles east of the Black Hills. Pre-Dakota erosion beveled all older rock units and removed many of the intervening beds younger than the Madison. Oil tests indicate that less than 200 feet of strata separate the Madison and Dakota in northern South Dakota east of the Missouri River; this is in marked contrast to the 1800 feet of intervening beds near Rapid City. It is believed that in a zone east of the Missouri River in northern South Dakota and adjacent North Dakota, water which has moved through the limestone more than 150 miles from the Black Hills moves upward into the basal part of the Dakota Sandstone. Much of the water developed in the area of major water use from the Dakota Sandstone has moved a relatively short distance through this formation. The chemical character and artesian pressure of water in the Dakota are influenced significantly by recharge from the Madison Group. West of the zone of recharge the water is highly mineralized and largely of a sodium chloride type. Along the zone of recharge and toward the southeast corner of South Dakota, an area of natural discharge, the water generally is of the calcium sulfate type. North of the Precambrian Sioux Quartzite and east of the calcium sulfate water is an area which has sodium sulfate water. It is inferred that this change results from natural base-exchange softening of the calcium sulfate water as it moves eastward through the Dakota Sandstone.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[163:NTORTT]2.0.CO;2","usgsCitation":"Swenson, F.A., 1968, New theory of recharge to the artesian basin of the Dakotas: Geological Society of America Bulletin, v. 79, no. 2, p. 163-182, https://doi.org/10.1130/0016-7606(1968)79[163:NTORTT]2.0.CO;2.","productDescription":"20 p.","startPage":"163","endPage":"182","costCenters":[],"links":[{"id":386441,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"North Dakota, South Dakota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -104.04052734375,\n 43.02071359427862\n ],\n [\n -96.43798828125,\n 43.02071359427862\n ],\n [\n -96.43798828125,\n 49.03786794532644\n ],\n [\n -104.04052734375,\n 49.03786794532644\n ],\n [\n -104.04052734375,\n 43.02071359427862\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"79","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Swenson, F. A.","contributorId":71622,"corporation":false,"usgs":true,"family":"Swenson","given":"F.","email":"","middleInitial":"A.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":817457,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70209028,"text":"70209028 - 1968 - Flow Structure and Composition of the Southern Coulee, Mono Craters, California—A Pumiceous Rhyolite Flow","interactions":[],"lastModifiedDate":"2020-03-11T18:31:29","indexId":"70209028","displayToPublicDate":"1968-01-01T18:24:50","publicationYear":"1968","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Flow Structure and Composition of the Southern Coulee, Mono Craters, California—A Pumiceous Rhyolite Flow","docAbstract":"The Southern Coulee is the southernmost and largest of the four Recent pumiceous rhyolitic coulees, or stubby flows, of the Mono Craters, eastern California. It is one of the youngest volcanic deposits of the Mono Craters and is largely bare and uneroded. The coulee is 3.6 km long and averages 1.2 km in width and 75 m in thickness. It was protruded from a north-trending fissure beneath the crest of the Mono Craters ridge. About two-thirds of the lava flowed west and one-third flowed east.
The coulee has three main parts: the dome, located over the orifice, where flow was about vertical; the flow, where movement was lateral; and the talus slope, which surrounds the coulee and formed from the advancing steep-flow front. In addition, three small areas of air-fall pumice ash occur on the coulee and appear to be remnants of an ash eruption that took place during an early phase of the coulee eruption.
Three distinctive lithologic units based on rock density related to the degree of vesicularity have been mapped: a unit of lowest density (average ρ = 0.65); a unit of intermediate density (average ρ = 1.20); and a unit of highest density (average ρ = 1.75). The contacts between the units are abrupt despite the fact that core drilling has shown the coulee to be a jumbled mass of blocks down to a depth of at least 45 m. The two less dense units, which consist of highly inflated thick-bedded pumice, form two connecting boat-shaped bodies along the entire south margin of the coulee. These units are probably not over 25 m thick and are underlain by the unit of highest density, which appears to form the rest of coulee. The dense unit consists of thin- to medium-bedded dense pumice and lesser amounts of obsidian. The above distribution of the lithologic units in the coulee was probably caused by the eruption of rocks characteristic of all the units from, the southern part of the north-trending fissure, while only rocks of the unit of highest density erupted from the northern part. The protrusion of the coulee involved several subordinate and, in places, interfering streams that had slightly different courses and levels. This complex flow resulted in a modification or disruption of the original spatial relations of the lithologic units, as they erupted from the orifice.
The petrographic and chemical data indicate a uniform composition for the lava that belies its heterogeneous aspect. The lava is composed almost entirely of clear glass (average nD = 1.488 ± 0.001), and contains only trace amounts of microlites and cristobalite-sanidine spherulites. Eight chemical anlyses show a silica range from 74.7 to 76.2 percent and indicate a rhyolite composition of the sodipotassic subrang. This composition is characteristic of glassy-fluidal rhyolites.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Studies in Volcanology","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM116-p415","usgsCitation":"Loney, R.A., 1968, Flow Structure and Composition of the Southern Coulee, Mono Craters, California—A Pumiceous Rhyolite Flow, chap. of Studies in Volcanology, v. 116, p. 415-440, https://doi.org/10.1130/MEM116-p415.","productDescription":"27 p.","startPage":"415","endPage":"440","costCenters":[],"links":[{"id":373149,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Mono Craters, Southern Coulee","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.2071533203125,\n 37.63815995799935\n ],\n [\n -118.79104614257811,\n 37.63815995799935\n ],\n [\n -118.79104614257811,\n 37.899239630600185\n ],\n [\n -119.2071533203125,\n 37.899239630600185\n ],\n [\n -119.2071533203125,\n 37.63815995799935\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Loney, R. A.","contributorId":90757,"corporation":false,"usgs":true,"family":"Loney","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":784577,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70006258,"text":"ofr68b - 1968 - Flood of June 7, 1967, in the Wapsinonoc Creek Basin, Iowa","interactions":[],"lastModifiedDate":"2016-02-22T11:08:49","indexId":"ofr68b","displayToPublicDate":"1968-01-01T16:39:00","publicationYear":"1968","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":"68","chapter":"B","title":"Flood of June 7, 1967, in the Wapsinonoc Creek Basin, Iowa","docAbstract":"An outstanding flood occurred in the Wapsinonoc Creek basin in east-central Iowa on June 7, 1967. The flood was the result of rainfall totaling from 4 to 13 inches in about 14 hours on the night of June 6 and the morning of June 7. The storm was nearly centered over the 180·square mile basin. The resulting peak discharges ranged from about 1.9 to about 4.3 times the 50-year recurrence interval flood. A peak discharge of 27,400 cubic feet per second was measured from 161 square miles of the basin. This and other peak discharges for drainage areas larger than 40 square miles were among the greatest recorded in the last 50 years in eastern Iowa. Flood damage was light because the basin is used primarily for agriculture and the crops were in their early growth stage. 'There was no loss of human life attributed to the flood.
","language":"English","publisher":"U.S. Geological Survey, Water Resources Division","publisherLocation":"Iowa City, Iowa","doi":"10.3133/ofr68b","collaboration":"Prepared in cooperation with the Iowa State Highway Commission","usgsCitation":"Schwob, H.H., 1968, Flood of June 7, 1967, in the Wapsinonoc Creek Basin, Iowa: U.S. Geological Survey Open-File Report 68, 21 p., https://doi.org/10.3133/ofr68b.","productDescription":"21 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":264349,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/b/report-thumb.jpg"},{"id":264348,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1968/b/report.pdf","size":"2553","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Iowa","city":"West Liberty","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.26754760742186,\n 41.73289216878352\n ],\n [\n -91.22016906738281,\n 41.70777900286713\n ],\n [\n -91.19682312011719,\n 41.6872711837914\n ],\n [\n -91.16661071777342,\n 41.66214019382183\n ],\n [\n -91.14463806152344,\n 41.64880139835668\n ],\n [\n -91.15287780761719,\n 41.62827478065122\n ],\n [\n -91.16798400878906,\n 41.6154423246811\n ],\n [\n -91.15013122558594,\n 41.599013054830216\n ],\n [\n -91.1267852783203,\n 41.58925619641459\n ],\n [\n -91.10000610351562,\n 41.581038750695754\n ],\n [\n -91.11579895019531,\n 41.56819689811343\n ],\n [\n -91.11236572265625,\n 41.54918627087084\n ],\n [\n -91.1432647705078,\n 41.54404730359805\n ],\n [\n -91.16043090820312,\n 41.53068407713936\n ],\n [\n -91.16867065429688,\n 41.51577568269484\n ],\n [\n -91.18583679199219,\n 41.50240661583931\n ],\n [\n -91.18583679199219,\n 41.48234783935022\n ],\n [\n -91.20643615722656,\n 41.478232450820364\n ],\n [\n -91.22016906738281,\n 41.46125371076149\n ],\n [\n -91.26274108886719,\n 41.45765158819396\n ],\n [\n -91.30050659179688,\n 41.4597099684453\n ],\n [\n -91.34307861328125,\n 41.46742831254425\n ],\n [\n -91.37809753417969,\n 41.47411680095253\n ],\n [\n -91.42753601074219,\n 41.485434209241745\n ],\n [\n -91.43508911132812,\n 41.49366381024536\n ],\n [\n -91.44058227539062,\n 41.5173180896782\n ],\n [\n -91.44401550292969,\n 41.54301946112854\n ],\n [\n -91.4337158203125,\n 41.56357320617609\n ],\n [\n -91.46049499511719,\n 41.59541859437006\n ],\n [\n -91.46324157714844,\n 41.625195224114876\n ],\n [\n -91.43646240234375,\n 41.64520971221468\n ],\n [\n -91.42959594726562,\n 41.66983439613616\n ],\n [\n -91.43852233886719,\n 41.6980386041929\n ],\n [\n -91.4666748046875,\n 41.71085461169185\n ],\n [\n -91.45637512207031,\n 41.72879273042403\n ],\n [\n -91.42753601074219,\n 41.741090260654076\n ],\n [\n -91.39045715332031,\n 41.75031186312044\n ],\n [\n -91.351318359375,\n 41.764141783336456\n ],\n [\n -91.29570007324219,\n 41.75184866809371\n ],\n [\n -91.26754760742186,\n 41.73289216878352\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a1132e4b0c8380cd53f08","contributors":{"authors":[{"text":"Schwob, Harlan H.","contributorId":23974,"corporation":false,"usgs":true,"family":"Schwob","given":"Harlan","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":354167,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221430,"text":"70221430 - 1968 - Geologic implications of aeromagnetic data for the eastern continental margin of the United States","interactions":[],"lastModifiedDate":"2021-06-16T12:23:30.849564","indexId":"70221430","displayToPublicDate":"1968-01-01T12:01:56","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"Geologic implications of aeromagnetic data for the eastern continental margin of the United States","docAbstract":"An aeromagnetic survey extending from the Gulf of Maine to the tip of Florida was conducted by the U. S. Naval Oceanographic Office between 1964 and 1966. Flight traverses were flown in a northwesterly direction at right angles to the geologic grain. The flight lines were approximately 800 km long and had an 8-km separation. The survey traversed part of the New England, Piedmont, and Coastal Plain provinces and extended some 320 km beyond the continental shelf into the Atlantic Ocean. Despite the wide flight-line spacing, numerous geological and structural features became apparent from this survey. Interpretation of these features was aided by using the available gravity and seismic data in addition to the State and Provincial geologic maps. The residual aeromagnetic map shows a continuous magnetic high on or near the continental slope as far south as the 31st parallel. At about the 36th parallel, this east-coast magnetic anomaly splits into two branches, and both of them parallel the 850-fathom contour. At the 31st parallel, the outer branch of the anomaly swings westward and crosses the coastline near Brunswick, Georgia. This continuous magnetic anomaly may result from an igneous intrusive body that parallels the edge of the pre-Paleozoic continental landmass. These magnetic data suggest that Florida and part of Georgia were added to the paleo-continent in pre-Paleozoic time. Landward from the east-coast anomaly, the magnetic field is quite variable, whereas oceanward it has an extremely small gradient. The absence of magnetic anomalies east of the continental slope suggests that in this region layer 2 may be composed of metamorphosed basalt. The characteristic magnetic patterns observed over the Piedmont and New England provinces extend oceanward to the east-coast anomaly.
","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1439970","usgsCitation":"Taylor, P., Zietz, I., and Dennis, L.S., 1968, Geologic implications of aeromagnetic data for the eastern continental margin of the United States: Geophysics, v. 33, no. 5, p. 755-780, https://doi.org/10.1190/1.1439970.","productDescription":"26 p.","startPage":"755","endPage":"780","costCenters":[],"links":[{"id":386498,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Eastern United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -69.3017578125,\n 47.517200697839414\n ],\n [\n -70.1806640625,\n 46.5286346952717\n ],\n [\n -71.3671875,\n 45.24395342262324\n ],\n [\n -74.794921875,\n 45.02695045318546\n ],\n [\n -76.2451171875,\n 44.24519901522129\n ],\n [\n -79.189453125,\n 43.51668853502906\n ],\n [\n -78.8818359375,\n 42.74701217318067\n ],\n [\n -82.6611328125,\n 41.83682786072714\n ],\n [\n -82.8369140625,\n 37.85750715625203\n ],\n [\n -83.5400390625,\n 36.70365959719456\n ],\n [\n -88.2861328125,\n 34.84987503195418\n ],\n [\n -89.912109375,\n 30.06909396443887\n ],\n [\n -80.771484375,\n 25.005972656239187\n ],\n [\n -78.837890625,\n 25.3241665257384\n ],\n [\n -68.6865234375,\n 39.198205348894795\n ],\n [\n -66.4892578125,\n 44.74673324024678\n ],\n [\n -67.3681640625,\n 45.644768217751924\n ],\n [\n -68.291015625,\n 47.39834920035926\n ],\n [\n -69.3017578125,\n 47.517200697839414\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"33","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Taylor, Patrick","contributorId":172618,"corporation":false,"usgs":false,"family":"Taylor","given":"Patrick","email":"","affiliations":[],"preferred":false,"id":817742,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":817743,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dennis, Leonard S.","contributorId":260351,"corporation":false,"usgs":false,"family":"Dennis","given":"Leonard","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":817744,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70206753,"text":"70206753 - 1968 - Overlapping plutonism, volcanism, and tectonism in the boulder batholith region, western Montana","interactions":[],"lastModifiedDate":"2024-09-24T18:39:03.087816","indexId":"70206753","displayToPublicDate":"1968-01-01T08:09:09","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2711,"text":"Memoir of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Overlapping plutonism, volcanism, and tectonism in the boulder batholith region, western Montana","docAbstract":"It is well known that the Boulder batholith region experienced intensive plutonism, volcanism, and tectonism that all began in Late Cretaceous time, after at least 700 m.y. of structural and igneous inactivity except for sporadic epeirogeny. Recent stratigraphic, structural, paleontologic, arid, especially, radiometric evidence makes it possible to date these dynamic events rather closely. The time relations that are revealed do not form a simple sequence of volcanism-folding-thrusting-batholith emplacement, as has often been supposed, but involve an intertwined complex.
Significant volcanism began ∼ 85 m.y. ago in late Coniacian or early Santonian time, with deposition of the thick, local tuffaceous Slim Sam Formation. Volcanism climaxed from 77 to 79 m.y. ago, in early Campanian time, when the region was buried under at least 10,000 feet of calc-alkalic volcanic and volcaniclastic rocks, which included many sheets of welded tuff - the Elkhorn Mountains Volcanics -, and a vast amount of contemporaneous ash was airborne beyond the region. Major volcanism ceased ∼ 73 m.y. ago, late in the Campanian, not to recur until early Eocene time, ∼ 50 m.y. ago.
The bulk of the batholith was emplaced beneath and within the volcanic edifice in early and middle Campanian time, during a 6 m.y. span from 78 to 72 m.y. ago, and some leucocratic masses were intruded during the next few million years, so that the whole batholith was emplaced within about 10 m.y.
Folding at and near the site of the batholith began in late Coniacian or Santonian time and culminated before middle Campanian time; the main folding north and east of the batholith was post-Campanian, probably Maestrichtian. Thrusting began before middle Santonian time, and recurred intermittently well into the Maestrichtian, or even a little later.
Thus volcanism, plutonism, folding, and thrusting began and ended within a few million years of each other, during the last 20 m.y. of the Cretaceous. Major folding, thrusting, and volcanism started about the same time, though not always at the same places, and a little earlier than plutonism. In any given locality, volcanism ended before major folding; the climax of plutonism followed the climax of volcanism; thrusting preceded and accompanied plutonism near the batholith, but followed plutonism farther away; thrusting ended a little later than folding. These dynamic processes so closely related in time and space must also be genetically related in the Boulder batholith region. Gilluly's (1965) conclusion that the orogeny which produced the great Cretaceous thrusts of Montana was \"essentially without plutonic associations\" is not tenable.
","language":"English","publisher":"Geological Society of American","doi":"10.1130/MEM116-p557","usgsCitation":"Robinson, G., Klepper, M.R., and Obradovich, J.D., 1968, Overlapping plutonism, volcanism, and tectonism in the boulder batholith region, western Montana: Memoir of the Geological Society of America, v. 116, p. 557-576, https://doi.org/10.1130/MEM116-p557.","productDescription":"20 p.","startPage":"557","endPage":"576","costCenters":[],"links":[{"id":462214,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","city":"Helena, Boulder, Deer Lodge, Butte","otherGeospatial":"boulder batholith","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -112.01934814453125,\n 46.60982785835103\n ],\n [\n -112.57827758789062,\n 46.5720787149159\n ],\n [\n -112.72247314453124,\n 46.380096460287824\n ],\n [\n -112.7197265625,\n 46.059891147620725\n ],\n [\n -112.50274658203125,\n 46.01603873833416\n ],\n [\n -112.36129760742188,\n 46.21785176740299\n ],\n [\n -112.16903686523436,\n 46.308047059262954\n ],\n [\n -112.02209472656249,\n 46.605110653248275\n ],\n [\n -112.01934814453125,\n 46.60982785835103\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Robinson, G.D.","contributorId":26350,"corporation":false,"usgs":true,"family":"Robinson","given":"G.D.","email":"","affiliations":[],"preferred":false,"id":775677,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Klepper, M. R.","contributorId":64278,"corporation":false,"usgs":true,"family":"Klepper","given":"M.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":775678,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Obradovich, J. D.","contributorId":48966,"corporation":false,"usgs":true,"family":"Obradovich","given":"J.","middleInitial":"D.","affiliations":[],"preferred":false,"id":775679,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2013,"text":"wsp1839L - 1968 - Geology and ground-water resources of Fillmore County, Nebraska, with a section on chemical quality of the water","interactions":[],"lastModifiedDate":"2023-11-02T20:09:09.399812","indexId":"wsp1839L","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","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":"1839","chapter":"L","title":"Geology and ground-water resources of Fillmore County, Nebraska, with a section on chemical quality of the water","docAbstract":"Fillmore County, an area 24 miles square, lies in the eastern part of the Nebraska loess plain. Although tributaries of the Big Blue River have eroded valleys into this plain, much of the original surface is intact. Broad flats and numerous shallow undrained depressions characterize the plain. \r\n\r\nThe county is underlain by unconsolidated deposits of Quaternary age to depths ranging from about 80 to 450 feet. The upper part of this depositional sequence consists largely of wind-deposited clayey silt, and the lower part of stream-deposited sand and gravel. In part of the county, deposits of glacial till also are included. The Quaternary deposits mantle an eroded surface of marine-deposited strata of Cretaceous age. \r\n\r\nThe lower deposits of Quaternary age are saturated and constitute a highly productive aquifer throughout much of the county. The saturated zone ranges from about 20 to 350 feet in thickness. Replenishment to this aquifer, derived principally from precipitation, is believed to average about 1.4 inches per year. Because the quantity of ground water pumped per year exceeds the average annual quantity of recharge, some of the water used for irrigation is from storage. Consequently, water levels in wells .are declining. This trend is likely to continue. \r\n\r\nThe ground water is of the calcium bicarbonate type and is hard, but it is chemically suitable for irrigation use on most soils in the county.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1839L","usgsCitation":"Keech, C.F., Dreeszen, V., and Petri, L.R., 1968, Geology and ground-water resources of Fillmore County, Nebraska, with a section on chemical quality of the water: U.S. Geological Survey Water Supply Paper 1839, Report: iv, 27 p.; 2 Plates: 45.81 x 36.50 inches and 37.00 x 16.49 inches, https://doi.org/10.3133/wsp1839L.","productDescription":"Report: iv, 27 p.; 2 Plates: 45.81 x 36.50 inches and 37.00 x 16.49 inches","costCenters":[],"links":[{"id":110026,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25053.htm","linkFileType":{"id":5,"text":"html"},"description":"25053"},{"id":27470,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1839l/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27471,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1839l/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137581,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1839l/report-thumb.jpg"},{"id":27469,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1839l/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nebraska","county":"Fillmore County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-97.3685,40.699],[-97.3678,40.4376],[-97.3686,40.3514],[-97.4827,40.3506],[-97.8206,40.351],[-97.8236,40.3505],[-97.8246,40.4367],[-97.8256,40.5243],[-97.826,40.6105],[-97.8245,40.6985],[-97.7111,40.6983],[-97.3685,40.699]]]},\"properties\":{\"name\":\"Fillmore\",\"state\":\"NE\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685b6d","contributors":{"authors":[{"text":"Keech, Charles Franklin","contributorId":44123,"corporation":false,"usgs":true,"family":"Keech","given":"Charles","email":"","middleInitial":"Franklin","affiliations":[],"preferred":false,"id":144529,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dreeszen, V. H.","contributorId":8825,"corporation":false,"usgs":true,"family":"Dreeszen","given":"V. H.","affiliations":[],"preferred":false,"id":144528,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Petri, L. R.","contributorId":48944,"corporation":false,"usgs":true,"family":"Petri","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":887471,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1000349,"text":"1000349 - 1968 - Movements of adult lake trout in Lake Superior","interactions":[],"lastModifiedDate":"2016-02-18T13:49:34","indexId":"1000349","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3624,"text":"Transactions of the American Fisheries Society","active":true,"publicationSubtype":{"id":10}},"title":"Movements of adult lake trout in Lake Superior","docAbstract":"Returns from mature lake trout (Salvelinus namaycush) tagged in western Lake Superior in 1959 and 1962-65 described here suggest that trout disperse widely from the spawning grounds after spawning and return in subsequent years. Although the data were not extensive, returns from lake trout tagged near Keweenaw Point in 1950 and off Marquette, Michigan, in 1952 suggested similar movement. Loftus stated that river-spawning lake trout of eastern Lake Superior returned annually to the same spawning streams. Movements of lake trout must be understood to manage and evaluate the rehabilitation of lake trout stocks in Lake Superior, especially when the trout move across interstate and international boundaries and are subject to different fishing regulations and fishing pressures.
","language":"English","publisher":"Wiley","doi":"10.1577/1548-8659(1968)97[481:MOALTI]2.0.CO;2","usgsCitation":"Rahrer, J.F., 1968, Movements of adult lake trout in Lake Superior: Transactions of the American Fisheries Society, v. 97, no. 4, p. 481-484, https://doi.org/10.1577/1548-8659(1968)97[481:MOALTI]2.0.CO;2.","productDescription":"4 p.","startPage":"481","endPage":"484","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":128662,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"97","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b482d","contributors":{"authors":[{"text":"Rahrer, Jerold F.","contributorId":76679,"corporation":false,"usgs":true,"family":"Rahrer","given":"Jerold","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":308436,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}