{"pageNumber":"1606","pageRowStart":"40125","pageSize":"25","recordCount":40783,"records":[{"id":1690,"text":"wsp1898A - 1969 - Stage-discharge characteristics of a Weir in a sand-channel stream","interactions":[],"lastModifiedDate":"2012-02-02T00:05:14","indexId":"wsp1898A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"1898","chapter":"A","title":"Stage-discharge characteristics of a Weir in a sand-channel stream","docAbstract":"A unique relation between water-surface elevation and water discharge usually does not exist for sand-channel streams. The relation is affected by changes in bed roughness and changes in bed elevation because of scour and fill. An artificial control on a sand-channel stream must control both the resistance to flow and the bed elevation in order to stabilize the relation between water-surface elevation and water discharge. \r\n\r\nThe weir (control structure) in the Rio Grande conveyance channel near Bernardo, N. Mex., was designed on the basis of a model study and field data (Harris and Richardson, 1964). About 72 percent of the measurements used to define the base relation between water-surface elevation and water discharge falls within plus or minus 5 percent of the mean relation for the prototype. The stage-discharge relation is not affected by backwater for values of submergence less than 90 percent. There is no consistent relation between the ratio of measured discharge to rated discharge and submergence for values of submergence greater than 90 percent. \r\n\r\nThe control does not restrict the channel capacity to less than the stated design capacity of 2,000 cubic feet per second. When the control is drowned out, or ineffective, the relation of water-surface elevation to water discharge is virtually the same as that prior to construction of the control for discharges greater than 1,500 cubic feet per second. When the control is not drowned out--that is, free-fall conditions exist--the water-surface elevation for a discharge of 2,000 cubic feet per second is greater than the minimum elevation, but is less than the maximum elevation that occurred at that discharge prior to construction. \r\n\r\nThe model study was only partially successful in predicting the operating characteristics of the prototype. Some of the differences between prototype operation and model predictions may exist because the prototype was not built exactly as recommended on the basis of the model study. In general, the prototype has operated somewhat better than the model predicted.","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/wsp1898A","usgsCitation":"Gonzalez, D.D., Scott, C., and Culbertson, J.K., 1969, Stage-discharge characteristics of a Weir in a sand-channel stream: U.S. Geological Survey Water Supply Paper 1898, iii, 29 p., https://doi.org/10.3133/wsp1898A.","productDescription":"iii, 29 p.","costCenters":[],"links":[{"id":137040,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1898a/report-thumb.jpg"},{"id":26775,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1898a/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e478fe4b07f02db48a1b7","contributors":{"authors":[{"text":"Gonzalez, Don D.","contributorId":49774,"corporation":false,"usgs":true,"family":"Gonzalez","given":"Don","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":143978,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Scott, C.H.","contributorId":101634,"corporation":false,"usgs":true,"family":"Scott","given":"C.H.","email":"","affiliations":[],"preferred":false,"id":143979,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Culbertson, James K.","contributorId":31371,"corporation":false,"usgs":true,"family":"Culbertson","given":"James","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":143977,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1078,"text":"wsp1859F - 1969 - Geohydrology and water utilization in the Willcox Basin, Graham and Cochise Counties, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1859F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"1859","chapter":"F","title":"Geohydrology and water utilization in the Willcox Basin, Graham and Cochise Counties, Arizona","docAbstract":"The Willcox basin is an area of interior drainage in the northern part of Sulphur Springs Valley, Cochise and Graham Counties, Ariz. The basin comprises about 1,500 square miles, of which the valley floor occupies about 950 square miles. \r\n\r\nThe basin probably formed during middle and late Tertiary time, when the area was subjected to large-scale faulting accompanied by the uplift of the mountain ranges that presently border it. During and after faulting, large quantities of alluvium were deposited in the closed basin. \r\n\r\nThe rocks in the basin are divided into two broad groups--the rocks of the mountain blocks, of Precambrian through Tertiary age, and the rocks of the basin, of Tertiary and Quaternary age. The mountain blocks consist of igneous, metamorphic, and sedimentary rocks; the water-bearing characteristics of these rocks depend primarily on their degree of weathering and fracturing. Even in areas where these rocks are fractured and jointed, only small amounts of water have been developed. The rocks of the basin consist of moderately consolidated alluvium, poorly consolidated alluvium, and unconsolidated alluvium. The water-bearing characteristics of the moderately and poorly consolidated alluvium are not well known. The unconsolidated alluvium underlies most of the valley floor and consists of two facies, stream deposits and lake beds associated with the old playa. The lenticular sand and gravel layers interbedded in silt- and clay-size material of the unconsolidated alluvium constitute the principal aquifer in the basin. The other aquifers, which yield less water, consist of beds of poorly to moderately consolidated sand- and gravel-size material; these beds occur in both the poorly consolidated and moderately consolidated alluvium. \r\n\r\nIn the Stewart area the median specific capacity of wells per 100 feet of saturated unconsolidated alluvium was 20 gallons per minute, and in the Kansas Settlement area the specific capacity of wells penetrating the poorly and moderately consolidated alluvium, undifferentiated, was only 7.4 gallons per minute per 100 feet of saturated material penetrated. The aquifer in the Kansas Settlement area is much less permeable but more homogeneous than the aquifer in the Stewart area. The coefficient of transmissibility of the aquifers, which was estimated from the specific-capacity data, ranged from 58,000 to 160,000 gal. tons per day per foot. \r\n\r\nPrior to extensive ground-water pumpage, the ground-water system probably was in equilibrium, with discharge equaling recharge. At that time, ground water moved toward the playa, where it was discharged by transpiration and evaporation. The estimate of the evapotranspiration in the playa area before large-scale development was about 75,000 acre-feet per year. On the basis of estimates of coefficients of transmissibility of the aquifer and on the basis of the water-table configuration, underflow toward the playa was computed to be about 54,000 acre-feet per year. \r\n\r\nBy 1963, large-scale pumping had caused marked changes in the shape of the piezometric surface; large cones of depression had developed, and ground-water movement was toward the centers of pumping. The cones of depression caused by large-scale pumping have since expanded, and water-level declines have been measured in the recharge areas along the mountain fronts. \r\n\r\nGround water has been used for irrigation since 1910. In 1928, about 4,000 acre-feet of ground water was pumped, and by 1963 180,000 acre-feet per year was being pumped. An estimated 1,860,000 acre-feet of water has been pumped for irrigation in the Willcox basin through 1963; 680,000 acre-feet from the Stewart area, 990,000 acre-feet from the Kansas Settlement area, and 190,000 acre-feet from the Pearce-Cochise area. In the Sierra Bonita Ranch area and the north playa area, ground-water withdrawal for irrigation through 1963 was small. From the spring of 1952 to the spring of 1964 water-level declines resulting from the ","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1859F","usgsCitation":"Brown, S., and Schumann, H.H., 1969, Geohydrology and water utilization in the Willcox Basin, Graham and Cochise Counties, Arizona: U.S. Geological Survey Water Supply Paper 1859, 32 p. :maps (3 fold. in pocket), https://doi.org/10.3133/wsp1859F.","productDescription":"32 p. :maps (3 fold. in pocket)","costCenters":[],"links":[{"id":138054,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1859f/report-thumb.jpg"},{"id":25785,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25786,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859f/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25787,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1859f/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25788,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1859f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8b50","contributors":{"authors":[{"text":"Brown, S. G.","contributorId":46914,"corporation":false,"usgs":true,"family":"Brown","given":"S. G.","affiliations":[],"preferred":false,"id":143141,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schumann, Herbert H.","contributorId":30964,"corporation":false,"usgs":true,"family":"Schumann","given":"Herbert","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143140,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":4919,"text":"pp606 - 1969 - Revision of some of Girty's invertebrate fossils from the Fayetteville Shale (Mississippian) of Arkansas and Oklahoma","interactions":[],"lastModifiedDate":"2015-10-21T10:16:21","indexId":"pp606","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"606","title":"Revision of some of Girty's invertebrate fossils from the Fayetteville Shale (Mississippian) of Arkansas and Oklahoma","docAbstract":"

J.n 1910, G. H. Girty published a paper on the fauna of the Fayetteville Shale of northern Arkansas and northeastern Oklahoma in which he described 110 new taxa of fossil invertebrates. He did not, however, designate any type specimens or divulge the localities at which •the fossils were collected, nor did he illustrate the species. The present study is designed to fill the gaps in information on some of these species and to bring them as far as possible up to date and in line with the modern scheme of classification.

\n

This report deals with the corals, pelecypods, _gastropods, trilobites, and ostracodes. It does not include the brachiopods and bryozoans. The study has been performed by specialists of the U.S. Geological Survey who are contributing separate parts to the volume.

\n

 

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp606","usgsCitation":"Gordon, M., Sando, W.J., Pojeta, J., Yochelson, E.L., and Sohn, I.G., 1969, Revision of some of Girty's invertebrate fossils from the Fayetteville Shale (Mississippian) of Arkansas and Oklahoma: U.S. Geological Survey Professional Paper 606, iii, 59 p.; 8 Plates; 1 Map: 21.62 x 12.87 inches, https://doi.org/10.3133/pp606.","productDescription":"iii, 59 p.; 8 Plates; 1 Map: 21.62 x 12.87 inches","numberOfPages":"94","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":251792,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0606/report-thumb.jpg"},{"id":247317,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0606/report.pdf","size":"9886","linkFileType":{"id":1,"text":"pdf"}},{"id":310255,"rank":301,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0606/plate-9.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Arkansas, Oklahoma","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -97.1630859375,\n 35.65729624809628\n ],\n [\n -97.1630859375,\n 37.00255267215955\n ],\n [\n -92.6806640625,\n 37.00255267215955\n ],\n [\n -92.6806640625,\n 35.65729624809628\n ],\n [\n -97.1630859375,\n 35.65729624809628\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a14e4b07f02db602b54","contributors":{"authors":[{"text":"Gordon, Mackenzie Jr.","contributorId":13225,"corporation":false,"usgs":true,"family":"Gordon","given":"Mackenzie","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":576292,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sando, William J.","contributorId":47851,"corporation":false,"usgs":true,"family":"Sando","given":"William","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":576293,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pojeta, John Jr.","contributorId":44514,"corporation":false,"usgs":true,"family":"Pojeta","given":"John","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":576294,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Yochelson, Ellis L.","contributorId":90802,"corporation":false,"usgs":true,"family":"Yochelson","given":"Ellis","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":576295,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Sohn, I. G.","contributorId":70751,"corporation":false,"usgs":true,"family":"Sohn","given":"I.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":576296,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":55893,"text":"ofr6953 - 1969 - Digital computer modeling for estimating mine-drainage problems, Piceance Creek basin, northwestern Colorado","interactions":[],"lastModifiedDate":"2014-07-15T11:30:30","indexId":"ofr6953","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-53","title":"Digital computer modeling for estimating mine-drainage problems, Piceance Creek basin, northwestern Colorado","docAbstract":"No abstract available.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ofr6953","usgsCitation":"Coffin, D.L., and Bredehoeft, J.D., 1969, Digital computer modeling for estimating mine-drainage problems, Piceance Creek basin, northwestern Colorado: U.S. Geological Survey Open-File Report 69-53, 20 p., https://doi.org/10.3133/ofr6953.","productDescription":"20 p.","numberOfPages":"20","costCenters":[],"links":[{"id":181535,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b464c","contributors":{"authors":[{"text":"Coffin, Donald L.","contributorId":90696,"corporation":false,"usgs":true,"family":"Coffin","given":"Donald","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":254429,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bredehoeft, John D.","contributorId":86747,"corporation":false,"usgs":true,"family":"Bredehoeft","given":"John","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":254428,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":2234,"text":"wsp1879H - 1969 - Water quality and discharge of streams in the Lehigh River Basin, Pennsylvania","interactions":[],"lastModifiedDate":"2017-06-21T11:04:08","indexId":"wsp1879H","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"1879","chapter":"H","title":"Water quality and discharge of streams in the Lehigh River Basin, Pennsylvania","docAbstract":"The Lehigh River, 100 miles long, is the second largest tributary to the Delaware River. It drains 1,364 square miles in four physiographic provinces. The Lehigh River basin includes mountainous and forested areas, broad agricultural valleys and areas of urban and industrial development. In the headwaters the water is of good quality and has a low concentration of solutes. Downstream, some tributaries receive coal-mine drainage and become acidic; others drain areas underlain by limestone and acquire alkaline characteristics. The alkaline streams neutralize and dilute the acid mine water where they mix. The dissolved-oxygen content of river water, which is high in the upper reaches of the stream, is reduced in the lower reaches because of lower turbulence, higher temperature, and the respiration of organisms. The Lehigh is used for public supply, recreation, waterpower, irrigation, and mining and other industrial purposes.\r\n\r\n Because the river is shallow in its upper reaches, most of the water comes in contact with the atmosphere as it churns over rocks and around islets and large boulders. Aeration of the water is rapid. When water that was low in dissolved-oxygen concentration was released from the lower strata of the Francis E. Walter Reservoir in June 1966, it quickly became aerated in the Lehigh River, and for 40 miles downstream from the dam the water was nearly saturated with oxygen.\r\n\r\n Most of the river water requires only moderate treatment for industrial use and public distribution throughout the Lehigh River valley. At times, however, some segments of the main river and its tributaries transport industrial wastes and acid coal-mine drainage. Usually the relatively high concentrations of solutes in water and the ensuing damage caused to quality by such waste discharges are more extensive and prolonged during droughts and other periods of low streamflow.\r\n\r\n For many years the Lehigh River flow has been continuously measured and its water chemically analyzed. Since May 1966 an instrument installed by the U.S. Geological Survey at Easton, Pa., has continuously recorded such water-quality parameters as specific conductance, temperature, and dissolved oxygen content.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1879H","usgsCitation":"McCarren, E.F., and Keighton, W.B., 1969, Water quality and discharge of streams in the Lehigh River Basin, Pennsylvania: U.S. Geological Survey Water Supply Paper 1879, iv, 48 p., https://doi.org/10.3133/wsp1879H.","productDescription":"iv, 48 p.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":137749,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1879h/report-thumb.jpg"},{"id":27993,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1879h/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5f9c5d","contributors":{"authors":[{"text":"McCarren, Edward F.","contributorId":106472,"corporation":false,"usgs":true,"family":"McCarren","given":"Edward","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":144865,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Keighton, Walter B.","contributorId":81877,"corporation":false,"usgs":true,"family":"Keighton","given":"Walter","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":144864,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":38830,"text":"pp529D - 1969 - Atlantic continental shelf and slope of the United States - Color of marine sediments","interactions":[],"lastModifiedDate":"2024-10-25T14:43:46.753707","indexId":"pp529D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"529","chapter":"D","title":"Atlantic continental shelf and slope of the United States - Color of marine sediments","docAbstract":"

A systematic examination of the regional color distribution of the upper sediment layer on the Atlantic continental margin between Nova Scotia and southern Florida reveals that brown, dark green, and yellow predominate on the shelf north of Cape Hatteras, whereas olive, gray, and yellow predominate to the south. Color is affected by composition. texture, physiography, and geological events in the recent past. Many of the color patterns on the shelf are more closely related to Pleistocene and Holocene sedimentary events than to modern dispersal processes. Relict color patterns occur in areas such as Georges and Browns Banks, which were exposed during lower stands of sea level. Linear but discontinuous belts of yellow sediment on the outer shelf and along the shelf break south of Cape Hatteras are probably also related to strandline features formed during the Pleistocene low stands of sea level and during the transgressive advance of the Holocene sea.

Color patterns on the continental slope and rise and on the Blake Plateau, unlike those on the shelf, are arranged in linear belts that trend parallel or subparallel to the shelf break. Major trends vary di redly with depth, ranging from olive and green at the top of the slope, through light gray and pale yellowish brown, to brown and yellow at. the top of the continental rise. These trends are probably related to the oxidation-reduction Potential of the environment, which results from a balance between the rate of deposition and the rate of bacterial decomposition of organic matter deposited with the sediment. Isolated areas of color on the slope and rise seem to be due to the slumping of sediment masses downslope and to the exposure of pre-Holocene outcrops. Red Pleistocene till masses, which were once exposed on the Scotian Shelf during the glacial epoch, may have been reworked during the Holocene rise in sea level. This may explain why 'brown and reddish-brown sediments are found at progressively shallower depths northeastward on the rise and slope off the Gulf of Maine and Nova Scotia.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp529D","usgsCitation":"Stanley, D., 1969, Atlantic continental shelf and slope of the United States - Color of marine sediments: U.S. Geological Survey Professional Paper 529, Report: iii, 15 p.; 1 Plate: 18.50 x 33.00 inches, https://doi.org/10.3133/pp529D.","productDescription":"Report: iii, 15 p.; 1 Plate: 18.50 x 33.00 inches","costCenters":[],"links":[{"id":120116,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0529d/report-thumb.jpg"},{"id":65761,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0529d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65762,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0529d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","otherGeospatial":"Atlantic continental shelf","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -61.951131406124944,\n 44.656140898792216\n ],\n [\n -65.03271055868028,\n 46.6747751769158\n ],\n [\n -68.09301659384751,\n 48.53700763232774\n ],\n [\n -85.39748164610373,\n 28.3802471692038\n ],\n [\n -80.39211999326048,\n 23.782933097067072\n ],\n [\n -61.951131406124944,\n 44.656140898792216\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aaee4b07f02db66c7bf","contributors":{"authors":[{"text":"Stanley, D.J.","contributorId":107356,"corporation":false,"usgs":true,"family":"Stanley","given":"D.J.","email":"","affiliations":[],"preferred":false,"id":220508,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":38817,"text":"pp543I - 1969 - Tectonics of the March 27, 1964, Alaska earthquake","interactions":[{"subject":{"id":38817,"text":"pp543I - 1969 - Tectonics of the March 27, 1964, Alaska earthquake","indexId":"pp543I","publicationYear":"1969","noYear":false,"chapter":"I","title":"Tectonics of the March 27, 1964, Alaska earthquake"},"predicate":"IS_PART_OF","object":{"id":70048225,"text":"pp543 - 1966 - The Alaska earthquake, March 27, 1964: regional effects","indexId":"pp543","publicationYear":"1966","noYear":false,"title":"The Alaska earthquake, March 27, 1964: regional effects"},"id":1}],"isPartOf":{"id":70048225,"text":"pp543 - 1966 - The Alaska earthquake, March 27, 1964: regional effects","indexId":"pp543","publicationYear":"1966","noYear":false,"title":"The Alaska earthquake, March 27, 1964: regional effects"},"lastModifiedDate":"2022-06-28T18:18:07.763935","indexId":"pp543I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"543","chapter":"I","title":"Tectonics of the March 27, 1964, Alaska earthquake","docAbstract":"The March 27, 1964, earthquake was accomp anied by crustal deformation-including warping, horizontal distortion, and faulting-over probably more than 110,000 square miles of land and sea bottom in south-central Alaska. Regional uplift and subsidence occurred mainly in two nearly parallel elongate zones, together about 600 miles long and as much as 250 miles wide, that lie along the continental margin. From the earthquake epicenter in northern Prince William Sound, the deformation extends eastward 190 miles almost to long 142° and southwestward slightly more than 400 miles to about long 155°. It extends across the two zones from the chain of active volcanoes in the Aleutian Range and Wrangell Mountains probably to the Aleutian Trench axis.\n\nUplift that averages 6 feet over broad areas occurred mainly along the coast of the Gulf of Alaska, on the adjacent Continental Shelf, and probably on the continental slope. This uplift attained a measured maximum on land of 38 feet in a northwest-trending narrow belt less than 10 miles wide that is exposed on Montague Island in southwestern Prince William Sound. Two earthquake faults exposed on Montague Island are subsidiary northwest-dipping reverse faults along which the northwest blocks were relatively displaced a maximum of 26 feet, and both blocks were upthrown relative to sea level. From Montague Island, the faults and related belt of maximum uplift may extend southwestward on the Continental Shelf to the vicinity of the Kodiak group of islands. To the north and northwest of the zone of uplift, subsidence forms a broad asymmetrical downwarp centered over the Kodiak-Kenai-Chugach Mountains that averages 2½ feet and attains a measured maximum of 7½ feet along the southwest coast of the Kenai Peninsula. Maximum indicated uplift in the Alaska and Aleutian Ranges to the north of the zone of subsidence was l½ feet. Retriangulation over roughly 25,000 square miles of the deformed region in and around Prince William Sound shows that vertical movements there were accompanied by horizontal distortion, involving systematic shifts of about 64 feet in a relative seaward direction. Comparable horizontal movements are presumed to have affected those parts of the major zones of uplift and subsidence for which retriangulation data are unavailable.\n\nRegional vertical deformation generated a train of destructive long-period seismic sea waves in the Gulf of Alaska as well as unique atmospheric and ionospheric disturbances that were recorded at points far distant from Alaska. Warping resulted in permanent tilt of larger lake basins and temporary reductions in discharge of some major rivers. Uplift and subsidence relative to sea level caused profound modifications in shoreline morphology with attendant catastrophic effects on the nearshore biota and costly damage to coasta1 installations. Systematic horizontal movements of the land relative to bodies of confined or semiconfined water may have caused unexplained short-period waves—some of which were highly destructive—observed during or immediately after the earthquake at certain coastal localities and in Kenai Lake. Porosity increases, probably related to horizontal displacements in the zone of subsidence, were reflected in lowered well-water levels and in losses of surface water.\n\nThe primary fault, or zone of faults, along which the earthquake occurred is not exposed at the surface on land. Focal-mechanism studies, when considered in conjunction with the pattern of deformation and seismicity, suggest that it was a complex thrust fault (megathrust) dipping at a gentle angle beneath the continental margin from the vicinity of the Aleutian Trench. Movement on the megathrust was accompanied by subsidiary reverse faulting, and perhaps wrench faulting, within the upper plate. Aftershock distribution suggests movement on a segment of the megathrust, some 550–600 miles long and 110–180 miles wide, that underlies most of the major zone of uplift and the seaward part of the major zone of subsidence.\n\nAccording to the postulated model, the observed and inferred tectonic displacements that accompanied the earthquake resulted primarily from (1) relative seaward displacement and uplift of the seaward part of the block by movement along the dipping megathrust and subsidiary faults that break through the upper plate to the surface, and (2) simultaneous elastic horizontal extension and vertical attenuation (subsidence) of the crustal slab behind the upper plate. Slight uplift inland from the major zones of deformation presumably was related to elastic strain changes resulting from the overthrusting; however, the data are insufficient to permit conclusions regarding its cause.\n\nThe belt of seismic activity and major zones of tectonic deformation associated with the 1964 earthquake, to a large extent, lie between and parallel to the Aleutian Volcanic Arc and the Aleutian Trench, and are probably genetically related to the arc. Geologic data indicate that the earthquake-related tectonic movements were but the most recent pulse in an episode of deformation that probably began in late Pleistocene time and has continued intermittently to the present. Evidence for progressive coastal submergence in the deformed region for several centuries preceding the earthquake, in combin1ation with transverse horizontal shortening indicated by the retriangulation data, suggests pre-earthquake strain directed at a gentle angle downward beneath the arc. The duration of strain accumulation in the epicentral region, as interpreted from the time interval during which the coastal submergence occurred, probably is 930–1,360 years.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Regional effects (Professional Paper 543)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp543I","usgsCitation":"Plafker, G., 1969, Tectonics of the March 27, 1964, Alaska earthquake: U.S. Geological Survey Professional Paper 543, Report: viii, 74 p.; 2 Plates: 27.08 x 21.87 inches and 16.09 x 20.66 inches, https://doi.org/10.3133/pp543I.","productDescription":"Report: viii, 74 p.; 2 Plates: 27.08 x 21.87 inches and 16.09 x 20.66 inches","numberOfPages":"88","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":402614,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4593.htm","linkFileType":{"id":5,"text":"html"}},{"id":277849,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0543i/index.html"},{"id":65741,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264156,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264155,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122539,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0543i/report-thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -141.2,51.8 ], [ -141.2,64.0 ], [ -174.1,64.0 ], [ -174.1,51.8 ], [ -141.2,51.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6858cd","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":220493,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3207,"text":"wsp1591D - 1969 - Considerations involved in evaluating mathematical modeling of urban hydrologic systems","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"wsp1591D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"1591","chapter":"D","title":"Considerations involved in evaluating mathematical modeling of urban hydrologic systems","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1591D","usgsCitation":"Dawdy, D.R., 1969, Considerations involved in evaluating mathematical modeling of urban hydrologic systems: U.S. Geological Survey Water Supply Paper 1591, 1 v. (issued as seperate chapters) :ill. ;24 cm. ;18 p., https://doi.org/10.3133/wsp1591D.","productDescription":"1 v. (issued as seperate chapters) :ill. ;24 cm. ;18 p.","costCenters":[],"links":[{"id":138134,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1591d/report-thumb.jpg"},{"id":30197,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1591d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b12e4b07f02db6a2f95","contributors":{"authors":[{"text":"Dawdy, David R.","contributorId":75125,"corporation":false,"usgs":true,"family":"Dawdy","given":"David","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":146432,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3658,"text":"cir608 - 1969 - Scientific or rule-of-thumb techniques of ground-water management--Which will prevail?","interactions":[],"lastModifiedDate":"2017-06-25T13:03:53","indexId":"cir608","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"608","title":"Scientific or rule-of-thumb techniques of ground-water management--Which will prevail?","docAbstract":"Emphasis in ground-water development, once directed largely to quantitatively minor (but sociologically vital) service of human and stock needs, is shifting: aquifers are treated as possible regulating reservoirs managed conjunctively with surface water. Too, emphasis on reducing stream pollution is stimulating interest in aquifers as possible waste-storage media. \r\n\r\nSuch management of aquifers requires vast amounts of data plus a much better understanding of aquifer-system behavior than now exists. Implicit in this deficiency of knowledge is a need for much new research, lest aquifers be managed according to ineffective rule-of-thumb standards, or even abandoned as unmanageable. \r\n\r\nThe geohydrologist's task is to define both internal and boundary characteristics of aquifer systems. Stratigraphy is a primary determinant of these characteristics, but stratigraphically minor features may make aquifers transcend stratigraphic boundaries. For example, a structurally insignificant fracture may carry more water than a major fault; a minor stratigraphic discontinuity may be a major hydrologic boundary. Hence, there is a need for ways of defining aquifer boundaries and quantifying aquifer and confining-bed characteristics that are very different from ordinary stratigraphic techniques. Among critical needs are techniques for measuring crossbed permeability; for extrapolating and interpolating point data on direction and magnitude of permeability in defining aquifer geometry; and for accurately measuring geochemical properties of water and aquifer material, and interpreting those measurements in terms of source of water, rate of movement, and waste-sorbing capacities of aquifers and of confining beds--in general, techniques adequate for predicting aquifer response to imposed forces whether static, hydraulic, thermal, or chemical. Only when such predictions can be made routinely can aquifer characteristics be inserted into a master model that incorporates both the hydrologic and the socioeconomic facts necessary to intelligent social actions involving water.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir608","usgsCitation":"McGuinness, C.L., 1969, Scientific or rule-of-thumb techniques of ground-water management--Which will prevail?: U.S. Geological Survey Circular 608, iii, 8 p. ;26 cm., https://doi.org/10.3133/cir608.","productDescription":"iii, 8 p. ;26 cm.","costCenters":[],"links":[{"id":30699,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1969/0608/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124739,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1969/0608/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ce4b07f02db5fceba","contributors":{"authors":[{"text":"McGuinness, Charles Lee","contributorId":101249,"corporation":false,"usgs":true,"family":"McGuinness","given":"Charles","email":"","middleInitial":"Lee","affiliations":[],"preferred":false,"id":147357,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":34790,"text":"b1271E - 1969 - Pecos National Monument, New Mexico: Its geologic setting","interactions":[],"lastModifiedDate":"2021-09-22T21:27:07.716549","indexId":"b1271E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1271","chapter":"E","title":"Pecos National Monument, New Mexico: Its geologic setting","docAbstract":"The ruins of the pueblos and missions of Pecos lie on the east bank of Glorieta Creek near its junction with the Pecos River at the south end of the Sangre de Cristo Mountains in north-central New Mexico. Here the Pecos River and Glorieta Creek have formed a broad rolling valley in which the red adobe walls of the mission church stand as a striking monument to a historic past.\r\n\r\nThis is beautiful country; the bright hues of red rocks are complemented by the varied greens of the junipers, pi?ons, and ponderosa pines. Northward the Sangre de Cristo Mountains stretch for miles in a blue mist toward the Truchas Peaks and forests of the Pecos Wilderness. A few miles south of the ruins the steep high escarpment of Glorieta Mesa marks, in a general way, the southern termination of the Rocky Mountain System, which here is represented by the Sangre de Cristos.\r\n\r\nThe escarpment of Glorieta Mesa has been formed largely by the Pecos River and its tributaries eroding the soft sedimentary layers. The Pecos flows southward from the high mountains in the north, parallels the mesa escarpment for 15 miles, and breaches the mesa near San Jose. About 1-1/2 miles southwest of the Pecos ruins at Cerro de Escobas is the highest point on Glorieta Mesa. It is the most conspicuous feature of the local landscape and rises to an elevation of 8,212 feet - 1,270 feet above the ruins. The slope of the escarpment here is very steep, rising 6 feet in every 10 horizontal feet.\r\n\r\nAlong the north side of the Glorieta Mesa escarpment is a 30-mile-long natural pass around the south end of the Sangre de Cristos that extends from Canoncito on the west to Starvation Peak on the east (fig. 1). The elevation of the pass is greater than 6,000 feet at all places, and it reaches its summit of 7,432 feet near the village of Glorieta near the west end of the pass. This pass has been used as a major travel route for more than 800 years by the Indians, Spanish, and Americans. The famous Santa Fe Trail passed through here and was superseded by the railroad, whose main-line tracks closely parallel the traces of the old wagon ruts. The modern four-lane divided highway, Interstate Highway I-25, carries high-speed automotive traffic through Glorieta Pass alongside the Santa Fe Railway. Glorieta Pass has been the locale of many important historical events, including the passage of Coronado's expedition in 1540-41; the construction of the two large mission churches at Pecos Pueblo; the capture and imprisonment of the men of the Texas Expedition in 1841; the passage of the American Army under General Kearny on its way to Santa Fe, Chihuahua, and California in 1846; and the Civil War Battle of Glorieta Pass in 1862.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to general geology, 1968","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1271E","usgsCitation":"Johnson, R.B., 1969, Pecos National Monument, New Mexico: Its geologic setting: U.S. Geological Survey Bulletin 1271, Report: iii, 11 p.; 1 Plate: 12.00 × 10.00 inches, https://doi.org/10.3133/b1271E.","productDescription":"Report: iii, 11 p.; 1 Plate: 12.00 × 10.00 inches","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":109683,"rank":699,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21363.htm","linkFileType":{"id":5,"text":"html"},"description":"21363"},{"id":62688,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1271e/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":62687,"rank":399,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1271e/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":167645,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1271e/report-thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Pecos National Monument","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.7170,\n 35.5137842234445\n ],\n [\n -105.64453124999999,\n 35.5137842234445\n ],\n [\n -105.64453124999999,\n 35.56853899134082\n ],\n [\n -105.7170,\n 35.56853899134082\n ],\n [\n -105.7170,\n 35.5137842234445\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad4e4b07f02db682ef5","contributors":{"authors":[{"text":"Johnson, Ross Byron","contributorId":37339,"corporation":false,"usgs":true,"family":"Johnson","given":"Ross","email":"","middleInitial":"Byron","affiliations":[],"preferred":false,"id":213590,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1143,"text":"wsp1608L - 1969 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","interactions":[{"subject":{"id":22722,"text":"ofr6436 - 1964 - Preliminary evaluation of corrosion and encrustation mechanisms in tube wells of the Indus Plains, West Pakistan","indexId":"ofr6436","publicationYear":"1964","noYear":false,"title":"Preliminary evaluation of corrosion and encrustation mechanisms in tube wells of the Indus Plains, West Pakistan"},"predicate":"SUPERSEDED_BY","object":{"id":1143,"text":"wsp1608L - 1969 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","indexId":"wsp1608L","publicationYear":"1969","noYear":false,"chapter":"L","title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan"},"id":1},{"subject":{"id":52566,"text":"ofr6745 - 1967 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plain, West Pakistan","indexId":"ofr6745","publicationYear":"1967","noYear":false,"title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plain, West Pakistan"},"predicate":"SUPERSEDED_BY","object":{"id":1143,"text":"wsp1608L - 1969 - Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","indexId":"wsp1608L","publicationYear":"1969","noYear":false,"chapter":"L","title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan"},"id":2}],"lastModifiedDate":"2012-02-02T00:05:18","indexId":"wsp1608L","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1608","chapter":"L","title":"Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan","docAbstract":"Seepage from rivers and irrigation canals has contributed to waterlogging and soil salinization problems in much of the Indus Plains of West Pakistan. These problems are being overcome in part by tube-well dewatering and deep leaching of salinized soils. The ground waters described here are anaerobic and some are supersaturated with troublesome minerals such as calcium carbonate (calcite) and iron carbonate (siderite). These waters are moderately corrosive to steel. Some wells contain sulfate-reducing bacteria, which catalyze corrosion, and pH-electrode potential relationships favorable to the solution of iron also are rather common. Corrosion is concentrated in the relatively active (anodic) saw slots of water-well filter pipes (screens), where metal loss is least tolerable. Local changes in chemical properties of the water, because of corrosion, apparently cause deposition of calcium carbonate, iron carbonate, and other minerals which clog the filter pipes. In some places well capacities are seriously reduced in very short periods of time. There appears to be no practicable preventive treatment for corrosion and encrustation in these wells. Even chemical sterilization for bacterial control has yielded poor results. Periodic rehabilitation by down-hole blasting or by other effective mechanical or chemical cleaning methods will prolong well life. It may be possible to repair severely damaged well screens by inserting perforated sleeves of plastic or other inert material. \r\n\r\nThe most promising approach to future, well-field development is to use filter pipes of epoxy-resin-bonded fiber glass, stainless steel, or other inert material which minimizes both corrosion and corrosion-catalyzed encrustation. Fiberglass plastic pipe appears to be the most economically practicable construction material at this time and already is being used with promising results.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1608L","usgsCitation":"Clarke, F., and Barnes, I., 1969, Evaluation and control of corrosion and encrustation in tube wells of the Indus Plains, West Pakistan: U.S. Geological Survey Water Supply Paper 1608, vi, 63 p. : ill., maps ;22 cm., https://doi.org/10.3133/wsp1608L.","productDescription":"vi, 63 p. : ill., maps ;22 cm.","costCenters":[],"links":[{"id":137622,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1608l/report-thumb.jpg"},{"id":25924,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1608l/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a50e4b07f02db629652","contributors":{"authors":[{"text":"Clarke, Frank Eldridge","contributorId":107255,"corporation":false,"usgs":true,"family":"Clarke","given":"Frank Eldridge","affiliations":[],"preferred":false,"id":143250,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barnes, Ivan","contributorId":56619,"corporation":false,"usgs":true,"family":"Barnes","given":"Ivan","email":"","affiliations":[],"preferred":false,"id":143249,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":12939,"text":"ofr6936 - 1969 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","interactions":[{"subject":{"id":12939,"text":"ofr6936 - 1969 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","indexId":"ofr6936","publicationYear":"1969","noYear":false,"title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California"},"predicate":"SUPERSEDED_BY","object":{"id":5758,"text":"pp882 - 1976 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","indexId":"pp882","publicationYear":"1976","noYear":false,"title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California"},"id":1}],"supersededBy":{"id":5758,"text":"pp882 - 1976 - Recent surface movements in the Baldwin Hills, Los Angeles County, California","indexId":"pp882","publicationYear":"1976","noYear":false,"title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California"},"lastModifiedDate":"2024-05-24T19:53:10.458712","indexId":"ofr6936","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-36","title":"Recent surface movements in the Baldwin Hills, Los Angeles County, California","docAbstract":"

The Baldwin Hills are located in the northwest part of the densely populated Los Angeles basin. They comprise one of several groups of isolated hills that extend along the northwest-trending Newport-Inglewood zone of folds and faults, a structural lineament identified with a series of very productive oil fields. In addition to being the site of the Inglewood oil field, these hills are the site of surface deformation that has been monitored for over 35 years. This record of deformation, which includes differential subsidence, horizontal displacements, and surface rupturing, forms one of the best documented examples of oilfield-associated surface deformation yet recognized. The deformation is described in detail, analyzed as to cause(s), and finally attributed largely or essentially entirely to the exploitation of the spatially-associated Inglewood oil field.

The Baldwin Hills are underlain by gently to moderately arched and conspicuously faulted Cenozoic sedimentary and volcanic rocks that overlie crystalline basement rocks at a depth of more than 10,000 feet. The Inglewood fault, a part of the northwest-trending Newport-Inglewood zone, diagonally transects the hills. Right-lateral displacements of 3,000-4,000 feet since middle or late Pliocene time and 1,500-2,000 feet during Quaternary time are indicated by offset structural and physio-graphic features; indications of vertical separations of up to about 200 feet during late Quaternary time occur locally.

Evidence of continuing deformation includes recognized seismicity and regional elevation changes. The M5-5 1/2 Inglewood earthquake of 1920, the largest local earthquake of record, is believed to have originated immediately southeast of the Baldwin Hills; it was apparently unassociated with surficial fault displacements. Leveling in and around the west and central Los Angeles basin has shown that lowland stations have been consistently subsiding, whereas foothill stations commonly have been rising. Several seemingly persistent basins of differential subsidence and a zone of positive movement, roughly coincident with the Newport-Inglewood zone, have also been identified in the northwest part of the basin.

A prominent, elliptically-shaped, northwest-trending subsidence bowl encompassing the northwest part of the Baldwin Hills, has been defined by repeated level circuits. Partial reconstruction of selected level circuits with respect to a common, relatively stable control point (Hollywood E-11), located on the edge of the subsidence bowl, has permitted evaluation of the subsidence since 1910 and 1911 at two points near the center of the bowl. Thus bench mark PBM 67 is estimated to have subsided approximately 4.324 feet between June 1910 and February 1963; and bench mark PBM 68 (the only bench mark within the subsidence bowl that was leveled prior to 1926 and has been repeatedly leveled since) subsided 3.846 feet between November 1911 and June 1962. Analysis of the available data indicates little if any elevation change at PBM 68 (or elsewhere throughout the Baldwin Hills-Inglewood area) associated with the Inglewood earthquake of 1920. Maximum subsidence of PBM 122 (which has remained very close to the center of subsidence since at . least 1950) between 1911 and 1963 is calculated to have been 5.67 feet.

Horizontal displacements (with respect to a north-south base line about 3 miles east of the hills) of six triangulation points within the subsidence bowl have been measured for various periods between 1934 and 1963. Displacements have been generally toward the center of subsidence and almost precisely perpendicular to the immediately adjacent isobases of equal elevation change. Maximum movement has been recorded at triangulation point Baldwin Aux, which was displaced 2.21 feet between 1934 and 1961; horizontal displacements of three additional points ranged from 0.95 foot to 1.85 feet between 1936 and 1961. Displacements of 0.10-0.29 foot were recorded at all six monuments during the period 1961-1963.

\"Earth cracks\" and surficial fault displacements were recognized in the Baldwin Hills at least as early as 1957. The cracks are relatively straight, generally continuous fractures confined to the structural block east of the Inglewood fault; they are concentrated in two areas centering on (1) the Baldwin Hills Reservoir and (2) the Stocker Street-LaBrea Avenue-Overhill Drive intersection. The cracks trend north to north-northeast and are nearly everywhere parallel to or coincident with minor faults and joints, and are generally orthogonal to radii emanating from the center of subsidence. Differential movement along the cracks has been almost entirely dip slip along steep to nearly vertical surfaces, and generally down-dropped toward the center of subsidence. Cumulative displacements have been as much as 6 or 7 inches. Rates of displacement have ranged widely, and the movement has generally occurred as creep or very small discrete jumps. A probable exception is the several inches of differential movement that is believed to have occurred along a crack through the floor of the Baldwin Hills Reservoir on or about December 14, 1963.

The contemporary surface movements are attributable to one or more of the following phenomena: (1). exploitation of the Inglewood oil field; (2) changes in the ground-water regimen; (3) compaction of sedimentary materials in response to surface loading; (4) tectonic activity.

The following considerations indicate that the differential subsidence is attributable largely or entirely to exploitation of the underlying Inglewood oil field: (1) the coincidence of the centers of the oil field, the producing structure, and the subsidence bowl; (2) the general correspondence between the pattern of subsidence and the outlines of the oil field; (3) the approximate coincidence between the initiation of production and the initiation of subsidence; (4) the generally linear relations between various measures of subsidence and liquid production from both the field as a whole and the exceptionally prolific Vickers zone in particular; (5) the sharp deceleration of subsidence in the eastern block of the field coincident with the initiation of full-scale water flooding there; (6) the many examples of oil fields In which both spatial and temporal associations between production and subsidence are recognized; (7) the many similarities of the subsidence-production relations in the Inglewood field to those in the Wilmington field, where the subsidence has been authoritatively attributed to oilfield operations; (8) the theoretical relation between subsidence or a tendency toward subsidence and increased effective pressure associated with underground fluid extraction.

Consideration of six possible explanations for the increasing rather than decreasing or constant rate of subsidence with respect to reservoir fluid pressure decline suggests that measured or calculated down-hole reservoir fluid pressure decline is non-representative of average or real fluid pressure decline away from producing wells. The near-linear relations between net-liquid production and subsidence are explained through analogy with a tightly confined artesian system of infinite areal extent, where production must derive from liquid expansion and/or reservoir compaction. Test data from compaction studies in two other oil fields yield estimates of ultimate compaction of the Vickers zone resulting from a total loss of fluid pressure; these estimates range over an order of magnitude. The best estimate, based on these data and considerations of late Cenozoic history in the Baldwin Hills area, is about 10 feet.

The centripetally-directed horizontal movements are considered attributable to exploitation of the Inglewood oil field on the basis of:
(1) their well-defined symmetrical and geometrical association with the differential subsidence; (2) the similarities between these associations and those developed in and around other subsiding oil fields; and (3) the mechanical compatibility of these movements with subsidence induced by the extraction of subsurface materials.

The earth cracks and surficial fault displacements are considered largely or entirely attributable to the exploitation of the Inglewood oil field on the basis of: (1) their spatial and temporal relations to both oil-field operations and the differential subsidence; (2) the similarities of these cracks and displacements to those generated in and around other oil fields and areas of subsurface materials extraction; and (3) surface strain patterns predicted from the measured vertical and horizontal surface movements. The cracks and displacements can i)e explained by an exploitation-based, elastic-rebound model which requires elastic compression of the sedimentary section in response to compaction-induced downdrag within those blocks around the periphery of the subsidence bowl. The measured displacements have been about one-quarter to one-half those predicted for a purely elastic system.

Analysis of: (1) the history of ground-water extraction within and around the Baldwin Hills; and (2) subsidence associated with water-level declines in sediments comparable with those in the Baldwin Hills, indicate that the surface movements can be no more than incidentally attributed to changes in ground-water conditions. Similarly, analysis of the history of natural and artificial changes in surface loading indicate that these movements are generally unassociated with changes in surface loading conditions.

Considerations of local geologic history and various tectonic associations indicate that it is very unlikely that the differential subsidence and horizontal movements are due to tectonic downwarping. There exists a far stronger prima facie argument for tectonic involvement in the earth cracking and associated fault displacements. This argument is disputed by; (1) the spatial and temporal relations of the earth cracks to, and their mechanical compatibility with, the nontectonic differential subsidence; (2) the absence of displacements on the Inglewood fault in conjunction with those along the conjugate earth cracks; (3) the probability that purely tectonic displaceMents would be characterized by oblique or strike slip; and (4) the absence of any clear temporal relation between crack growth and local seismicity, However, because as much as 10 percent of the local isobase gradient may be unexplained' by oil-field exploitation, a small fraction of this gradient, and thus the displacements among the southern group of cracks, may be attributable to tectonic activity. This fraction should have been insignificant in the presence of the strain pattern produced by nontectonic compaction of the underlying oil measures.

Because nearly all of the observed and measured surface movements can be fully explained as the products of oil-field operations, yet can be no more than incidentally attributed to changes in ground-water conditions, surface loading, or tectonic activity, we conclude that these movements are attributable largely or essentially entirely to the exploitation of the Inglewood oil field.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6936","usgsCitation":"Castle, R.O., and Yerkes, R.F., 1969, Recent surface movements in the Baldwin Hills, Los Angeles County, California: U.S. Geological Survey Open-File Report 69-36, xviii, 185 p., https://doi.org/10.3133/ofr6936.","productDescription":"xviii, 185 p.","costCenters":[],"links":[{"id":429278,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0036/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146998,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0036/report-thumb.jpg"}],"country":"United States","state":"California","county":"Los Angeles County","otherGeospatial":"Baldwin Hills","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.38187677397389,\n 34.0348739886972\n ],\n [\n -118.38187677397389,\n 33.97553856602411\n ],\n [\n -118.30144514525205,\n 33.97553856602411\n ],\n [\n -118.30144514525205,\n 34.0348739886972\n ],\n [\n -118.38187677397389,\n 34.0348739886972\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7ee4b07f02db648569","contributors":{"authors":[{"text":"Castle, Robert O.","contributorId":22741,"corporation":false,"usgs":true,"family":"Castle","given":"Robert","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":166993,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Yerkes, R. F.","contributorId":24754,"corporation":false,"usgs":true,"family":"Yerkes","given":"R.","middleInitial":"F.","affiliations":[],"preferred":false,"id":166994,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":13486,"text":"ofr6987 - 1969 - Evaluation of core data, physical properties, and oil yield USBM/AEC Colorado Core Hole no. 3 (Bronco BR-1)","interactions":[],"lastModifiedDate":"2012-02-02T00:06:37","indexId":"ofr6987","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-87","title":"Evaluation of core data, physical properties, and oil yield USBM/AEC Colorado Core Hole no. 3 (Bronco BR-1)","docAbstract":"USBM/AEC Colorado Core Hole No. 3 (Bronco BR-1) is located in the SW1/4SW1/4SW1/4 sec. 14, T. 1 N., R. 98 W., Rio Blanco County, Colorado. The collar is at a ground elevation of 6,356 feet. The hole was core drilled between depths of 964 and 3,325 feet with a total depth of 3,797 feet. The hole was drilled to investigate geologic, geophysical and hydrological conditions at a possible in situ oil-shale retorting experiment site. The drill hole passed through 1,157 feet of alluvium and the Evacuation Creek Member of the Green River Formation, 1,603 feet of the Parachute Creek Member and penetrated into the Garden Gulch Member of the Green River Formation. In-bole density log/oil yield ratio interpretation indicates that two oil-shale zones exist which yield more than 20 gallons of shale oil per ton of rock; an upper zone lying between 1,271 and 1,750 feet in depth and a lower zone lying between 1,900 and 2,964 feet. Halite (sodium chloride salt) is found between 2,140 and 2,185 feet and nahcolite (sodium bicarbonate salt) between 2,195 and 2,700 feet. Nahcolite was present at one time above 2,195 feet but has been subsequently dissolved out by ground water. The core can be divided into six structural units based upon degree of fracturing. A highly fractured interval is found between 1,646 and 1,899 feet, which coincides with the dissolution or leached nahcolite zone. Physical property tests made on core samples between 1,356 and 3,253 feet give average values of 11,988 psi for uniaxial compressive strength, 1.38 X 10[superscript]6[superscript] psi for static Young's modulus and 11,809 fps for compressional velocity.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6987","usgsCitation":"Ege, J.R., Carroll, R.D., Way, R., and Magner, J.E., 1969, Evaluation of core data, physical properties, and oil yield USBM/AEC Colorado Core Hole no. 3 (Bronco BR-1): U.S. Geological Survey Open-File Report 69-87, 25 p. ill. (some folded, col.), map ;29 cm., https://doi.org/10.3133/ofr6987.","productDescription":"25 p. ill. (some folded, col.), map ;29 cm.","costCenters":[],"links":[{"id":144724,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0087/report-thumb.jpg"},{"id":41955,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41956,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41960,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41961,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41962,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0087/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41957,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41958,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41959,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0087/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a09e4b07f02db5fae72","contributors":{"authors":[{"text":"Ege, John R.","contributorId":69534,"corporation":false,"usgs":true,"family":"Ege","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":167874,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carroll, R. D.","contributorId":53373,"corporation":false,"usgs":true,"family":"Carroll","given":"R.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":167873,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Way, R.J.","contributorId":17238,"corporation":false,"usgs":true,"family":"Way","given":"R.J.","email":"","affiliations":[],"preferred":false,"id":167872,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Magner, J. E.","contributorId":87131,"corporation":false,"usgs":true,"family":"Magner","given":"J.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":167875,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":15426,"text":"ofr69205 - 1969 - Meteoritic origin and consequent endogenic modification of large lunar craters - a study in analytic geomorphology","interactions":[],"lastModifiedDate":"2012-02-02T00:07:08","indexId":"ofr69205","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-205","title":"Meteoritic origin and consequent endogenic modification of large lunar craters - a study in analytic geomorphology","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr69205","usgsCitation":"Pike, R.J., 1969, Meteoritic origin and consequent endogenic modification of large lunar craters - a study in analytic geomorphology: U.S. Geological Survey Open-File Report 69-205, 404 p. ill. ;29 cm., https://doi.org/10.3133/ofr69205.","productDescription":"404 p. ill. ;29 cm.","costCenters":[],"links":[{"id":148632,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4fe4b07f02db6288e0","contributors":{"authors":[{"text":"Pike, Richard J. rpike@usgs.gov","contributorId":5753,"corporation":false,"usgs":true,"family":"Pike","given":"Richard","email":"rpike@usgs.gov","middleInitial":"J.","affiliations":[],"preferred":true,"id":171121,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23859,"text":"ofr70209 - 1969 - Perspective center determination","interactions":[],"lastModifiedDate":"2012-02-02T00:08:07","indexId":"ofr70209","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"70-209","title":"Perspective center determination","docAbstract":"This program determines coordinates of the perspective center of a stereoplotter projector by bringing two bundles of rays into a best fit coincidence in a space-resection solution. One of the bundles of rays is defined by the perspective center and the grid intersections on a grid plate. The other bundle of rays is defined by the perspective center and the projected grid intersections in the model space. \r\n\r\nThe program is used with the independent-model method of semianalytlcal aerotriangulation, which requires the coordinates of perspective centers. It may also be used in checking the calibration of stereoplotters.","language":"ENGLISH","publisher":"U.S. Geological Survey, Topographic Division,","doi":"10.3133/ofr70209","issn":"0094-9140","usgsCitation":"McLaurin, J., 1969, Perspective center determination: U.S. Geological Survey Open-File Report 70-209, 41 p. :ill. ;28 cm., https://doi.org/10.3133/ofr70209.","productDescription":"41 p. :ill. ;28 cm.","costCenters":[],"links":[{"id":155699,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1970/0209/report-thumb.jpg"},{"id":53079,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1970/0209/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b20e4b07f02db6abb09","contributors":{"authors":[{"text":"McLaurin, J.D.","contributorId":68348,"corporation":false,"usgs":true,"family":"McLaurin","given":"J.D.","email":"","affiliations":[],"preferred":false,"id":190871,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":53593,"text":"ofr69207 - 1969 - An iterative digital model for aquifer evaluation","interactions":[],"lastModifiedDate":"2012-02-02T00:11:24","indexId":"ofr69207","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-207","title":"An iterative digital model for aquifer evaluation","language":"ENGLISH","doi":"10.3133/ofr69207","usgsCitation":"Pinder, G.F., 1969, An iterative digital model for aquifer evaluation: U.S. Geological Survey Open-File Report 69-207, 35 leaves : ill. ; 28 cm., https://doi.org/10.3133/ofr69207.","productDescription":"35 leaves : ill. ; 28 cm.","costCenters":[],"links":[{"id":178361,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0207/report-thumb.jpg"},{"id":87479,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0207/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db6842aa","contributors":{"authors":[{"text":"Pinder, George Francis","contributorId":99964,"corporation":false,"usgs":true,"family":"Pinder","given":"George","email":"","middleInitial":"Francis","affiliations":[],"preferred":false,"id":247868,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":17964,"text":"ofr699 - 1969 - Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska","interactions":[{"subject":{"id":17964,"text":"ofr699 - 1969 - Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska","indexId":"ofr699","publicationYear":"1969","noYear":false,"title":"Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":39568,"text":"pp700D - 1970 - Geological Survey research 1970, Chapter D","indexId":"pp700D","publicationYear":"1970","noYear":false,"chapter":"D","title":"Geological Survey research 1970, Chapter D"},"id":1}],"supersededBy":{"id":39568,"text":"pp700D - 1970 - Geological Survey research 1970, Chapter D","indexId":"pp700D","publicationYear":"1970","noYear":false,"title":"Geological Survey research 1970, Chapter D"},"lastModifiedDate":"2024-01-17T19:39:16.691625","indexId":"ofr699","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"69-9","title":"Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska","docAbstract":"

An aeromagnetic map covering 480 square miles was compiled for the Nixon Fork district, which is located approximately 35 miles northeast of McGrath, Alaska. The survey was flown in search of concealed intrusive rocks which may have produced contact metamorphic deposits in limestone similar to the known lode deposits which have been the principal source of gold in the district.

The exposed quartz monzonite stocks with which the lode deposits are associated produce negative magnetic anomalies. Slight to moderately strong positive anomalies correlate with granitic intrusives in contact with Upper Cretaceous rocks in the Iditarod-Nixon Fork fault zone. No significant mineral deposits have been found in conjunction with these granitic bodies.

Positive anomalies, delineating buried intrusives, occur near the east and west boundaries of the mapped area. The nature of the westernmost intrusive is unknown.

An area of possible economic interest lies between Limestone Mountain and Whirlwind-Canyon Creeks in the eastern sector of the mapped area. An elliptical positive anomaly is superimposed on an elongate, slightly negative anomaly. This negative anomaly may represent an intrusive similar to the quartz monzonite with which the lode deposits are affiliated. The positive anomaly may be a near-vertical mafic dike intruded to within 50 feet of the surface of a limestone ridge. Limestone in the vicinity of the dike may be a favorable area for prospecting for lode deposits similar to the known gold-producing deposits of the district.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr699","usgsCitation":"Anderson, L.A., Reed, B.L., and Johnson, G.R., 1969, Preliminary geologic interpretation of aeromagnetic data in the Nixon Fork district, Alaska: U.S. Geological Survey Open-File Report 69-9, Report: ii, 6 p.; 1 Plate: 40.63 x 31.55 inches, https://doi.org/10.3133/ofr699.","productDescription":"Report: ii, 6 p.; 1 Plate: 40.63 x 31.55 inches","costCenters":[],"links":[{"id":149186,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0009/report-thumb.jpg"},{"id":424516,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0009/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":424515,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0009/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Alaska","otherGeospatial":"Nixon Fork district","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -156.21098975436422,\n 64.39363688486736\n ],\n [\n -156.0545619009912,\n 64.39363688486736\n ],\n [\n -156.0545619009912,\n 64.40237470471484\n ],\n [\n -156.21098975436422,\n 64.40237470471484\n ],\n [\n -156.21098975436422,\n 64.39363688486736\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -158.14993847514128,\n 64.4117874414261\n ],\n [\n -158.14993847514128,\n 63.40759602117143\n ],\n [\n -150.94307945964977,\n 63.40759602117143\n ],\n [\n -150.94307945964977,\n 64.4117874414261\n ],\n [\n -158.14993847514128,\n 64.4117874414261\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c2e1","contributors":{"authors":[{"text":"Anderson, Lennart A.","contributorId":106111,"corporation":false,"usgs":true,"family":"Anderson","given":"Lennart","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":178293,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reed, Bruce L.","contributorId":19928,"corporation":false,"usgs":true,"family":"Reed","given":"Bruce","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":178294,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Johnson, Gordon R.","contributorId":90725,"corporation":false,"usgs":true,"family":"Johnson","given":"Gordon","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":178295,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5673,"text":"pp666 - 1969 - Magnetic fields for a 4x6 prismatic model","interactions":[],"lastModifiedDate":"2012-02-02T00:05:54","indexId":"pp666","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"666","title":"Magnetic fields for a 4x6 prismatic model","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/pp666","usgsCitation":"Andreasen, G., and Zietz, I., 1969, Magnetic fields for a 4x6 prismatic model: U.S. Geological Survey Professional Paper 666, 9 p., https://doi.org/10.3133/pp666.","productDescription":"9 p.","costCenters":[],"links":[{"id":118034,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0666/report-thumb.jpg"},{"id":32192,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0666/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6492ea","contributors":{"authors":[{"text":"Andreasen, Gordon E.","contributorId":94272,"corporation":false,"usgs":true,"family":"Andreasen","given":"Gordon E.","affiliations":[],"preferred":false,"id":151409,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":151408,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1676,"text":"wsp1757K - 1969 - A ground-water reconnaissance of the Republic of Ghana, with a description of geohydrologic provinces","interactions":[],"lastModifiedDate":"2012-02-02T00:05:23","indexId":"wsp1757K","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","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":"1757","chapter":"K","title":"A ground-water reconnaissance of the Republic of Ghana, with a description of geohydrologic provinces","docAbstract":"This report gives a general summary of the availability and use of ground water and describes the occurrence of ground water in five major geohydrologic provinces lying in the eight administrative regions of Ghana. The identification and delineation of the geohydrologic provinces are based on their distinctive characteristics with respect to the occurrence and availability of ground water. \r\n\r\nThe Precambrian province occupies the southern, western, and northern parts of Ghana and is underlain largely by intrusive crystalline and metasedimentary rocks. The Voltaian province includes that part of the Voltaian sedimentary basin in central Ghana and is underlain chiefly by consolidated sandstone, mudstone, and shale. Narrow discontinuous bands of consolidated Devonian and Jurassic sedimentary rocks near the coast constitute the Coastal Block Fault province. \r\n\r\nThe Coastal Plain province includes semiconsolidated to unconsolidated sediments of Cretaceous to Holocene age that underlie coastal plain areas in southwestern and southeastern Ghana. The Alluvial province includes the Quaternary alluvial deposits in the principal river valleys and on the delta of the Volta River. Because of the widespread distribution of crystalline and consolidated sedimentary rocks of low permeability in the Precambrian, Voltaian, and Coastal Block Fault provinces, it is difficult to develop large or event adequate groundwater supplies in much of Ghana. On the other hand, small (1 to 50 gallons per minute) supplies of water of usable quality are available from carefully sited boreholes in most parts of the country. Also, moderate (50 to 200 gpm) supplies of water are currently (1964) obtained from small-diameter screened boreholes tapping sand and limestone aquifers in the Coastal Plain province in southwestern and southeastern Ghana, but larger supplies could be obtained through properly constructed boreholes. In the Alluvial province, unconsolidated deposits in the larger stream valleys that are now largely undeveloped offer desirable locations for shallow vertical or horizontal wells, which can induce infiltration from streams and yield moderate to large water supplies. \r\n\r\nThe principal factors that limit development of ground-water supplies in Ghana are (1) prevailing low permeability and water-yielding potential of the crystalline and consolidated sedimentary rocks that underlie most of the country, (2) highly mineralized ground water which appears to be widely distributed in the northern part of the Voltaian province, and (3) potential problems of salt-water encroachment in the Coastal Plain province in the Western Region and in the Keta area. \r\n\r\nOn the other hand, weathering has increased porosity and has thus substantially increased the water-yielding potential of the crystalline and consolidated sedimentary rocks in much of central and northern Ghana. Also, with proper construction and development, much larger yields than those now (1964) prevalent could be obtained from boreholes tapping sand and limestone aquifers in the Coastal Plain province.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1757K","usgsCitation":"Gill, H., 1969, A ground-water reconnaissance of the Republic of Ghana, with a description of geohydrologic provinces: U.S. Geological Survey Water Supply Paper 1757, iii, 38 p., https://doi.org/10.3133/wsp1757K.","productDescription":"iii, 38 p.","costCenters":[],"links":[{"id":138253,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1757k/report-thumb.jpg"},{"id":26751,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757k/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26752,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1757k/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26753,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1757k/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b45c0","contributors":{"authors":[{"text":"Gill, H.E.","contributorId":24330,"corporation":false,"usgs":true,"family":"Gill","given":"H.E.","email":"","affiliations":[],"preferred":false,"id":143958,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70112275,"text":"70112275 - 1969 - The geographic applications program of the U. S. Geological Survey","interactions":[],"lastModifiedDate":"2017-03-27T13:58:42","indexId":"70112275","displayToPublicDate":"1990-06-12T11:43:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3051,"text":"Photogrammetric Engineering","active":true,"publicationSubtype":{"id":10}},"title":"The geographic applications program of the U. S. Geological Survey","docAbstract":"

The fundamental objective of modern Geography is to improve man's level of living through a better understanding of man-environment inter actions. Related goals of the USGS program for applications of remote sensor data to Geographical research are: (1) the analysis and improvement of land use, with special emphasis on urban problems; and (2) more effective use of the total available energy budget, including insolation, mineral fuels, atomic energy, human resources, and mental energy, all of which are integrated into man-environment interactions. The collection of data through remote sensors in air craft and spacecraft is financed largely by funds from NASA, and is part of the much broader EROS Program of the Department of the Interior. Results to date have achieved much toward the identification of remote sensor signatures for Earth features and human activities, and toward evaluation of instruments for collecting essential information.

","language":"English","publisher":"American Society of Photogrammetry","publisherLocation":"Falls Church, VA","usgsCitation":"Gerlach, A.C., 1969, The geographic applications program of the U. S. Geological Survey: Photogrammetric Engineering, v. 35, no. 1, p. 58-60.","productDescription":"3 p.","startPage":"58","endPage":"60","numberOfPages":"3","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288477,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"35","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc58e4b0e83db6d0902b","contributors":{"authors":[{"text":"Gerlach, Arch C.","contributorId":78249,"corporation":false,"usgs":true,"family":"Gerlach","given":"Arch","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":494608,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207466,"text":"70207466 - 1969 - Interstitial water studies on small core samples, Deep Sea Drilling Project, Leg 1","interactions":[],"lastModifiedDate":"2019-12-19T16:46:01","indexId":"70207466","displayToPublicDate":"1969-12-31T16:41:16","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1997,"text":"Initial reports of the Deep Sea Drilling Project","active":true,"publicationSubtype":{"id":10}},"title":"Interstitial water studies on small core samples, Deep Sea Drilling Project, Leg 1","docAbstract":"

The most dramatic variations in pore water composition occurred in Holes 2 and 3 in the Gulf of Mexico. Both holes showed a strong increase in salinity with depth, evidently owing to diffusion from underlying salt bodies. However, on Challenger Knoll (Hole 2) a sharp drop in salinity was observed in the cap rock of the salt dome in which chloride fell to only 4.8 percent. The drop is attributed to production of fresh water during the formation of native sulfur.

Outside of the Gulf of Mexico, changes in total salinity with depth did not exceed a few percent, but differences in diagenetic modification of the ionic ratios of sea water were pronounced. In nondiapiric strata in the Gulf of Mexico (Hole 1) both magnesium and potassium were depleted in the pore waters, whereas in the open ocean holes (4, 5, 6, and 7), potassium appeared in excess. Water content (porosity) of the cores was irregular.

","language":"English","publisher":"National Science Foundation","doi":"10.2973/dsdp.proc.1.120.1969","usgsCitation":"Manheim, F.T., and Sayles, F., 1969, Interstitial water studies on small core samples, Deep Sea Drilling Project, Leg 1: Initial reports of the Deep Sea Drilling Project, v. 1, p. 403-410, https://doi.org/10.2973/dsdp.proc.1.120.1969.","productDescription":"11 p.","startPage":"403","endPage":"410","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":488839,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2973/dsdp.proc.1.120.1969","text":"Publisher Index Page"},{"id":370524,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Manheim, Frank T. 0000-0003-4005-4524","orcid":"https://orcid.org/0000-0003-4005-4524","contributorId":20770,"corporation":false,"usgs":true,"family":"Manheim","given":"Frank","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":778156,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sayles, F.L.","contributorId":77657,"corporation":false,"usgs":true,"family":"Sayles","given":"F.L.","email":"","affiliations":[],"preferred":false,"id":778157,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207273,"text":"70207273 - 1969 - The relationship between fluids in some fresh alpine-type ultramafics and possible modern serpentinization, western United States","interactions":[],"lastModifiedDate":"2019-12-15T13:35:58","indexId":"70207273","displayToPublicDate":"1969-12-31T13:35:23","publicationYear":"1969","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 relationship between fluids in some fresh alpine-type ultramafics and possible modern serpentinization, western United States","docAbstract":"

Calcium hydroxide waters issue from four partly serpentinized Alpine-type ultramafic bodies in the western United States. The occurrence of calcium-hydroxide-type water is restricted to fresh Alpine-type ultramafic rocks. The calcium hydroxide waters are unsaturated with Mg end-member olivine and pyroxene but supersaturated with Mg end-member brucite and serpentine and thus have chemical potentials to cause Serpentinization. The calcium hydroxide waters are isotopically similar to the common magnesium bicarbonate meteoric waters peculiar to ultramafic rocks and serpentinites. Some Serpentinization is apparently a near-surface phenomenon occurring at present. The Serpentinization takes place at nearly constant composition, except for loss of CaO. © 1969, The Geological Society of America, Inc.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[1947:TRBFIS]2.0.CO;2","issn":"00167606","usgsCitation":"Barnes, I., and O’Neil, J.R., 1969, The relationship between fluids in some fresh alpine-type ultramafics and possible modern serpentinization, western United States: Geological Society of America Bulletin, v. 80, no. 10, p. 1947-1960, https://doi.org/10.1130/0016-7606(1969)80[1947:TRBFIS]2.0.CO;2.","productDescription":"14 p. ","startPage":"1947","endPage":"1960","costCenters":[],"links":[{"id":370279,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"80","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Barnes, I.","contributorId":23678,"corporation":false,"usgs":true,"family":"Barnes","given":"I.","affiliations":[],"preferred":false,"id":777511,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"O’Neil, J. R.","contributorId":111576,"corporation":false,"usgs":true,"family":"O’Neil","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":777512,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011516,"text":"70011516 - 1969 - Shock and thermal metamorphism of basalt by nuclear explosion, Nevada test site","interactions":[],"lastModifiedDate":"2026-02-03T17:49:21.96302","indexId":"70011516","displayToPublicDate":"1969-12-26T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Shock and thermal metamorphism of basalt by nuclear explosion, Nevada test site","docAbstract":"Olivine trachybasalt metamorphosed by nuclear explosion is classified into categories of progressive metamorphism: (i) Weak. Plagioclase is microfractured, and augite cotainis fine twin lamellae. (ii) Moderate. Plagioclase is converted to glass, and mafic minerals show intragranular deformation (undulatory extinction, twin lamellae, and, possibly, deformation lamellae), but rock texture is preserved. (iii) Moderately strong. Plagioclase glass shows small-scale flow, mafic minerals are fractured and show intragranular deformation, and rocks contain tension fractures. (iv) Strong. Plagioclase glass is vesicular, augite is minutely fractured, and olivine is coarsely fragmented, shows mosaic extinction, distinctive lamellar structures, and is locally recrystallized. (v) Intense. Rocks are converted to inhomogeneous basaltic glass.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.166.3913.1615","issn":"00368075","usgsCitation":"James, O., 1969, Shock and thermal metamorphism of basalt by nuclear explosion, Nevada test site: Science, v. 166, no. 3913, p. 1615-1620, https://doi.org/10.1126/science.166.3913.1615.","productDescription":"6 p.","startPage":"1615","endPage":"1620","costCenters":[],"links":[{"id":221531,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Nevada test site","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -115.86148761030728,\n 36.28102420050834\n ],\n [\n -115.86148761030728,\n 35.73549986999858\n ],\n [\n -115.04699320065484,\n 35.73549986999858\n ],\n [\n -115.04699320065484,\n 36.28102420050834\n ],\n [\n -115.86148761030728,\n 36.28102420050834\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"166","issue":"3913","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b8e7be4b08c986b318975","contributors":{"authors":[{"text":"James, O.B.","contributorId":100526,"corporation":false,"usgs":true,"family":"James","given":"O.B.","email":"","affiliations":[],"preferred":false,"id":361301,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70206916,"text":"70206916 - 1969 - Experimental studies of pegmatite genesis: I. A model for the derivation and crystallization of granitic pegmatites","interactions":[],"lastModifiedDate":"2019-11-26T17:36:33","indexId":"70206916","displayToPublicDate":"1969-12-01T17:30:08","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Experimental studies of pegmatite genesis: I. A model for the derivation and crystallization of granitic pegmatites","docAbstract":"

The genesis of granitic igneous pegmatites is here considered in terms of a model conceived from results of field and laboratory studies and subsequently tested by means of experimental investigations. This model emphasizes the roles of water (and/or other relatively volatile substances), both as a dissolved constituent in granitic magmas and as the dominant constituent of a separate fluid phase that is in the supercritical state under most conditions of pegmatite formation. Pegmatite magma, as distinguished by a content of dissolved water that is high relative to the limit of solubility under existing confining pressure, can be formed either through partial melting of crustal materials or as rest-liquid in a cooling igneous body yielding dominantly anhydrous crystalline phases. Such granitic magma can be expected to consolidate according to the following three-fold sequence: 1. Crystallization from hydrous silicate melt, yielding anhydrous solid phases with or without OH-bearing phases. The product is characterized by normal phaneritic textures that generafly are coarse grained. It has been termed pegmatite in some occurrences, and granite in others. 2. Crystallization concomitantly from silicate melt and from a coexisting exsolved aqueous fluid of considerably lower viscosity, yielding giant-textured pegmatite along with much finer-grained, even aplitic, mineral aggregates. Segregation of these products can vary enormously in scale and degree. Partitioning of constituents between melt and aqueous fluid, rapid diffusion of constituents through the aqueous phase, and gravitational rising of this fluid through the system contribute to formation of pods, zones, and other rock units of unusual composition and texture. 3. Crystallization in the absence of silicate melt, yielding a wide variety of late-stage products. These include so-called \"pocket minerals\" and numerous mineral aggregates formed through exchanges of material among aqueous fluid and earlier-formed crystal-line phases. Development of pegmatite bodies can begin with either Step 1 or Step 2, but it is suggested that the processes involved in Step 2 are essential to the formation of all true pegmatites of igneous origin. The appearance of a second fluid phase, in general a supercritical aqueous fluid derived from the crystallizing melt, is regarded as the decisive event; it is promptly followed by fundamental changes in distribution and texture of the solid phases being formed. The processes can operate effectively in a fully closed system, and they also can modify the surrounding rocks if the system is open at any stage. Step 1 can include reactions between magma and earlier-formed crystals, but far more rapid and extensive exchanges of materials are subsequently effected by processes included in Steps 2 and 3; indeed, such exchanges also can account satisfactorily for pegmatites of metamorphic origin. Crystallization of most granitic magmas in the absence of a separate aqueous phase probably would begin within the temperature range 1,300°-650 ° C, the specific liquidus temperature depending mainly upon the amounts of volatile constituents held in solution at the time. This compositional factor also would be important in controlling the stage of crystallization-late, intermediate, or early-at which a separate aqueous fluid would make its appearance. Depending upon confining pressure as dictated by geologic conditions for a given system, the stage in crystallization represented by the presence of both silicate melt and aqueous fluid could begin within about the same temperature range of 1.300°-650 ° C. Exhaustion of the melt could occur within range extending downward to temperatures of 600C or even somewhat lower. Textural and structural features appear to be the most reliable indicators of the stages and fundamental processes involved in crystallization of both natural and synthetic pegmatites. The contrasting processes of crystallization from one fluid and from more than one fluid can operate over such broad P-T-X ranges that simple genetic pegmatite classifications based largely upon \"key minerals,\" presumed temperature or pressure intervals, or the presence or absence of supercritical conditions appear to be somewhat unrealistic. © 1969 Society of Economic Geologists, Inc.

","language":"English","publisher":"Society of Economic Geologists ","doi":"10.2113/gsecongeo.64.8.843","issn":"03610128","usgsCitation":"Jahns, R.H., and Burnham, C., 1969, Experimental studies of pegmatite genesis: I. A model for the derivation and crystallization of granitic pegmatites: Economic Geology, v. 64, no. 8, p. 843-864, https://doi.org/10.2113/gsecongeo.64.8.843.","productDescription":"22 p. ","startPage":"843","endPage":"864","costCenters":[],"links":[{"id":369688,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"64","issue":"8","noUsgsAuthors":false,"publicationDate":"1969-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Jahns, R. H.","contributorId":97961,"corporation":false,"usgs":true,"family":"Jahns","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":776248,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Burnham, C.W.","contributorId":220937,"corporation":false,"usgs":false,"family":"Burnham","given":"C.W.","email":"","affiliations":[],"preferred":false,"id":776249,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70223877,"text":"70223877 - 1969 - Mesozoic California and the underflow of Pacific mantle","interactions":[],"lastModifiedDate":"2021-09-10T20:41:55.668543","indexId":"70223877","displayToPublicDate":"1969-12-01T15:32:51","publicationYear":"1969","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":"Mesozoic California and the underflow of Pacific mantle","docAbstract":"

The Mesozoic evolution of California is interpreted as dominated by the underflow of oceanic mantle beneath the continental margin. Underflow during part of Late Cretaceous time of more than 2000 km of the eastern Pacific plate seems required by the marine magnetic data. Correspondingly, varied oceanic environments—abyssal hill, island arc, trench, oceanic crust, and upper mantle, perhaps also continental rise and abyssal plain—appear to be represented in the eugeosynclinal terranes of California. The rock juxtapositions accord with the concept that these materials were scraped off against the continent as the oceanic plate slid beneath it along Mesozoic Benioff seismic zones, which are now seen as serpentine belts separating profoundly different rock assemblages.

The chaotic Franciscan Formation of coastal California consists of deep-ocean Late Jurassic to Late Cretaceous sedimentary, volcanic, crustal, and mantle materials. As open-ocean abyssal oozes and the oceanic crust beneath them were swept into the Benioff-zone trench at the continental margin, they were covered by terrigenous clastic sediments, and the entire complex was carried beneath the correlative continental-shelf and continental-slope deposits (Great Valley sequence) and the older Mesozoic complexes.

The other eugeosynclinal terranes of California can be interpreted, albeit with less confidence, in similar terms of underflow of Pacific mantle. In the Klamath Mountains and northern Sierra Nevada, for example, Ordovician and Silurian ocean-floor materials, overlain by or juxtaposed against an Upper Silurian to Permian island arc, were swept in first to the continent, along with a large fragment of oceanic crust and mantle and another fragment of an old orogenic belt. This debris was followed by Permian and Triassic ocean-floor deposits. Late Triassic and Jurassic volcanic products from stocks and batholiths forming in the welded complexes lapped across both landward and oceanward sides of the region.

Reversal of Cenozoic extension, strike-slip faulting, and volcanic crustal growth in the western United States reveals a Cretaceous tectonic pattern strikingly like the modern pattern of the Andes, so the paleotectonic setting of North America can be inferred from the South American present. The Mesozoic batholiths of North America, like the late Cenozoic volcanic belt of the central Andes, are products of the same rapid motion of oceanic plates that carried oceanic sediments against the continent to form eugeosynclinal terranes. Magmas generated in the Benioff zones formed the batholiths and the volcanic fields which initially capped them.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1969)80[2409:MCATUO]2.0.CO;2","usgsCitation":"Hamilton, W., 1969, Mesozoic California and the underflow of Pacific mantle: Geological Society of America Bulletin, v. 80, no. 12, p. 2409-2429, https://doi.org/10.1130/0016-7606(1969)80[2409:MCATUO]2.0.CO;2.","productDescription":"21 p.","startPage":"2409","endPage":"2429","costCenters":[],"links":[{"id":389117,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"East Pacific Rise, Franciscan Formation, Klamath Mountains, North American continental plate, Pacific Ocean, Pacific plate, Sierra 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