{"pageNumber":"1610","pageRowStart":"40225","pageSize":"25","recordCount":40783,"records":[{"id":33791,"text":"b1246 - 1967 - Metalliferous lode deposits of Alaska","interactions":[],"lastModifiedDate":"2016-06-21T13:56:12","indexId":"b1246","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1246","title":"Metalliferous lode deposits of Alaska","docAbstract":"<p>An important factor in any rebirth of metal mining in Alaska will be a thorough appraisal of the metalliferous lodes already known in the State. Any such appraisal probably will depend, at least in part, on an inventory of these 1 deposits and a knowledge of their geology.</p>\n<p>This report summarizes from repoAs of Federal and State agencies published before August 31, 1965, the geology of Alaska's metal-bearing lodes, including their structural or stratigraphic control, host rock, mode of origin, kinds of .Q minerals, grade, past production, and extent of exploration. In addition, the lists of mineral occurrences that accompany the 35 mineral-deposit location maps constitute an inventory of the State's known lodes. A total of 692 localities where m&amp;alliferous deposits have been found are shown on the maps. The localities include 1,739 mines, prospects, and reported occurrences, of which 821 are described individually or otherwise cited in the text.</p>","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/b1246","usgsCitation":"Berg, H., and Cobb, E.H., 1967, Metalliferous lode deposits of Alaska: U.S. Geological Survey Bulletin 1246, Report: vi, 254 p.; Plate: 33.00 x 26.50 inches, https://doi.org/10.3133/b1246.","productDescription":"Report: vi, 254 p.; Plate: 33.00 x 26.50 inches","numberOfPages":"260","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":166560,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/b1246.PNG"},{"id":323083,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1246/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":61691,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1246/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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,{"id":2696,"text":"wsp1841 - 1967 - Geology and ground water of the Savannah River Plant and vicinity, South Carolina","interactions":[],"lastModifiedDate":"2022-03-22T20:03:39.563475","indexId":"wsp1841","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1841","title":"Geology and ground water of the Savannah River Plant and vicinity, South Carolina","docAbstract":"<p>The area described in this report covers approximately 2,600 square miles in west-central South Carolina and includes the site of the Savannah River Plant, a major production facility of the U.S. Atomic Energy Commission. The climate, surface drainage, and land forms of the study area are typical of the southern part of the Atlantic Coastal Plain. Precipitation is normally abundant and fairly evenly distributed throughout the year, and the mean annual temperature is moderately warm (64?F). The major streams that drain the area (the Savannah, Salkehatchie, and Edisto Rivers) have low gradients and flow in a southeasterly direction toward the Atlantic Ocean. Surface features of the area include narrow, flat-bottomed, steep-sided valleys and broad gently rolling interfluvial areas. Those parts of the Coastal Plain included within the report area can be subdivided into the Aiken Plateau, the Congaree Sandhills, and the Coastal Terraces. The area is underlain by a sequence of unconsolidated and partly consolidated sediments of Late Cretaceous, Tertiary, and Quaternary age. The unconsolidated sediments were deposited unconformably on a basement of igneous and metamorphic rocks of Precambrian and Paleozoic age and sedimentary rocks of Triassic age. The basement rocks are similar to the granite-diorite complex of the Charlotte Belt, the metamorphosed rocks of the Carolina Slate Belt, and the consolidated sediments of the Newark Group. The unconsolidated sediments strike about N. 60 ? E. and dip 6-20 feet per mile to the southeast. They form a wedge-shaped mass that increases in thickness toward the southeast to slightly more than 1,200 feet in the vicinity of Allendale, S.C., on the southeast or downdip side of the study area. The oldest or lowermost unconsolidated sedimentary unit, the Tuscaloosa Formation of Late Cretaceous age, is overlain in the subsurface by beds that are also probably Late Cretaceous in age and that herein are named the Ellenton Formation. The Upper Cretaceous deposits are, in turn, overlain by the, McBean Formation and the Congaree(?) Formation of middle Eocene age, the Barnwell Formation of late Eocene age, the Hawthorn Formation of early and middle Miocene age, and by fluvial and marine(?) terrace deposits of Pliocene(?), Pleistocene, and Recent age. In the mapped area, the Congaree(?) Formation includes undifferentiated rocks (mostly Congaree and Barnwell Formations and some Mcbean outliers). (See map explanation.) Structurally, the Upper Cretaceous sediments are overlapped to the northwest by Tertiary deposits. A preliminary geologic map of the general area is included in the report. The principal aquifer in the area is composed of the beds of medium to coarse sand and gravel contained in the Tuscaloosa and Ellenton Formations. Subordinate aquifers include deposits of sand and limestone of Tertiary and Quaternary age. The ground water in the principal aquifer occurs under water-table conditions in the outcrop area of the Tuscaloosa Formation in the northern and western parts of the study area, but it is under artesian pressure downdip in the southern and eastern parts of the study area. Contours drawn on the piezometric surface of the water in the principal aquifer indicate that water is recharged to the aquifer mainly by leakage through the overlying Tertiary formations. Likewise, the piezometric contours show that the outcrop area of the Tuscaloosa Formation functions chiefly as an area of discharge. Doubtless, water is also discharged from the aquifer by moving downdip to areas near the coast where the prevailing hydraulic gradient may favor the upward leakage of water through the upper confining beds. The hydraulic properties of the principal aquifer were determined by a series of pumping tests. The results indicate that the aquifer is highly productive and could supply 15 million gallons per day in the vicinity of the Savannah River Plant without exceeding the available drawdown.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1841","usgsCitation":"Siple, G.E., 1967, Geology and ground water of the Savannah River Plant and vicinity, South Carolina: U.S. Geological Survey Water Supply Paper 1841, Report: iv, 113 p.; 6 Plates: 33.00 × 29.50 inches or smaller, https://doi.org/10.3133/wsp1841.","productDescription":"Report: iv, 113 p.; 6 Plates: 33.00 × 29.50 inches or smaller","costCenters":[{"id":13634,"text":"South Atlantic Water Science 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George E.","contributorId":94282,"corporation":false,"usgs":true,"family":"Siple","given":"George","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":145626,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":2174,"text":"wsp1834 - 1967 - Geology and ground-water resources of Laramie County, Wyoming","interactions":[{"subject":{"id":52033,"text":"ofr4995 - 1949 - Progress report on the geology and ground-water resources of the Cheyenne area, Wyoming","indexId":"ofr4995","publicationYear":"1949","noYear":false,"title":"Progress report on the geology and ground-water resources of the Cheyenne area, Wyoming"},"predicate":"SUPERSEDED_BY","object":{"id":2174,"text":"wsp1834 - 1967 - Geology and ground-water resources of Laramie County, Wyoming","indexId":"wsp1834","publicationYear":"1967","noYear":false,"title":"Geology and ground-water resources of Laramie County, Wyoming"},"id":1}],"lastModifiedDate":"2022-02-01T22:54:13.04712","indexId":"wsp1834","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1834","title":"Geology and ground-water resources of Laramie County, Wyoming","docAbstract":"<p>Laramie County, an area of 2,709 square miles, is in the southeast corner of Wyoming. Rocks exposed there range in age from Precambrian to Recent. The most extensive aquifers in the county are the White River Formation of Oligocene age, which is as much as 500 feet thick and consists predominantly of siltstone ; the Arikaree Formation of Miocene age, which consists of as much as 450 feet of very fine grained to fine-grained sandstone; and the Ogallala Formation of Miocene and Pliocene age, which consists ,of as much as 330 feet of gravel, sand, silt, and some cobbles and boulders. These formations are capable of yielding large ,supplies of water locally. Terrace deposits of Quaternary age yield moderate .to large supplies of water in the southeastern and northeastern parts of the county. In the Federal well field, large yields of water from the White River Formation are obtained from gravel lenses. In the eastern part of the county near Pine Bluffs, large yields are obtained from openings in .the siltstone of the White River. Previous investigators reported that the large yields were obtained in areas where the formation is fractured and fissured. The authors of this report believe that .the large yields from siltstone in the White River Formation are from pipes, sometimes called natural tunnels, rather than from fractures ,or fissures. Little is known about the water-bearing properties of the pro-Tertiary aquifers in the county, but water derived from the pro-Tertiary formations would probably be of poor quality, except in the vicinity of the outcrop near the western edge of the county. Precipitation is the principal source of recharge to the ground-water reservoirs. About 5 percent of the annual precipitation, or about 108,400 acre-feet per year, is estimated to be recharged. Only a small amount of additional recharge is from streams. The general movement of ground water is eastward, and the average gradient of the water table is about 40 feet per mile. The total amount ,of ground water pumped from wells in Laramie County during 1964 is estimated to be 28,000 acre-feet; about 6,000 acre-feet was used for municipal and industrial supplies, about 17,000 acre-feet was used for irrigation in the Pine Bluffs-Carpenter area, and about 5,000 acre-feet was used for other purposes. The balance of the recharge (80,400 acre-feet) is estimated to be discharged by the following means: 20 percent by underflow, 20 percent by streamflow, and 60 percent by evapotranspiration. The coefficient of transmissibility of the Ogallala Formation, determined by averaging data from 28 pumping tests made in the Cheyenne municipal well field, is about 16,000 gallons per day per foot. However, this figure is an average of the more permeable zones, and the average coefficient of transmissibility of the Ogallala in the county is probably much less because of the heterogeneous character of the formation. A coefficient of transmissibility of 3,800 gallons per day per foot was calculated for the Ogallala, in the same vicinity that the pumping tests were made, by using a regional method of analysis. Although the average transmissibility of the Ogallala is considered to be low, large yields are obtained from gravel stringers and lenses in the formation. The maximum perennial yield from the Cheyenne well field is estimated to be about 1.6 billion gallons per year. Moderate to large yields of water can be obtained in the north-central part of the county where the saturated thickness of the Arikaree Formation, or combined Arikaree and Ogallala Formations, is 200 feet or more. Ground water has been developed throughout the county, but development has been intensive only in the Cheyenne municipal well fields near Cheyenne and Federal and in the Pine Bluffs lowland. The water level has been lowered as much as 40 feet in the Cheyenne well field and somewhat less in the Federal well field.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1834","usgsCitation":"Lowry, M.E., Crist, M.A., and Tilstra, J.R., 1967, Geology and ground-water resources of Laramie County, Wyoming: U.S. Geological Survey Water Supply Paper 1834, Report: iv, 71 p.;  2 Plates: 39.50 × 28.18 inches and 38.00 × 28.15 inches, https://doi.org/10.3133/wsp1834.","productDescription":"Report: iv, 71 p.;  2 Plates: 39.50 × 28.18 inches and 38.00 × 28.15 inches","costCenters":[],"links":[{"id":27786,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1834/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27785,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1834/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27787,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1834/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":110025,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25039.htm","linkFileType":{"id":5,"text":"html"},"description":"25039"},{"id":138197,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1834/report-thumb.jpg"}],"country":"United States","state":"Wyoming","county":"Laramie County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-104.6506,41.651],[-104.6491,41.5656],[-104.0521,41.5654],[-104.052,41.3949],[-104.0526,41.0236],[-104.0528,41.0017],[-104.1399,41.0019],[-104.4725,41.0027],[-104.4875,41.0027],[-104.5606,41.0028],[-104.5679,41.0028],[-104.6087,41.0046],[-104.6134,41.0048],[-104.6337,41.0056],[-104.6648,41.0047],[-104.6837,41.0041],[-104.7013,41.0035],[-104.83,40.9996],[-104.8341,40.9996],[-104.9385,40.9995],[-104.9425,40.9995],[-105.1109,40.9993],[-105.2763,40.9998],[-105.2774,41.6567],[-105.1706,41.6535],[-105.0575,41.6537],[-104.9419,41.6537],[-104.6506,41.651]]]},\"properties\":{\"name\":\"Laramie\",\"state\":\"WY\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685b2c","contributors":{"authors":[{"text":"Lowry, Marlin E.","contributorId":52552,"corporation":false,"usgs":true,"family":"Lowry","given":"Marlin","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144770,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crist, Marvin A.","contributorId":63376,"corporation":false,"usgs":true,"family":"Crist","given":"Marvin","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":144771,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Tilstra, John R.","contributorId":44897,"corporation":false,"usgs":true,"family":"Tilstra","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144769,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":1976,"text":"wsp1662D - 1967 - Specific yield: compilation of specific yields for various materials","interactions":[{"subject":{"id":52334,"text":"ofr6359 - 1963 - Compilation of specific yield for various materials","indexId":"ofr6359","publicationYear":"1963","noYear":false,"title":"Compilation of specific yield for various materials"},"predicate":"SUPERSEDED_BY","object":{"id":1976,"text":"wsp1662D - 1967 - Specific yield: compilation of specific yields for various materials","indexId":"wsp1662D","publicationYear":"1967","noYear":false,"chapter":"D","title":"Specific yield: compilation of specific yields for various materials"},"id":1}],"lastModifiedDate":"2014-04-29T08:30:19","indexId":"wsp1662D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1662","chapter":"D","title":"Specific yield: compilation of specific yields for various materials","docAbstract":"Specific yield is defined as the ratio of (1) the volume of water that a saturated rock or soil will yield by gravity to (2) the total volume of the rock or soft. Specific yield is usually expressed as a percentage. The value is not definitive, because the quantity of water that will drain by gravity depends on variables such as duration of drainage, temperature, mineral composition of the water, and various physical characteristics of the rock or soil under consideration. Values of specific yields nevertheless offer a convenient means by which hydrologists can estimate the water-yielding capacities of earth materials and, as such, are very useful in hydrologic studies. \n\nThe present report consists mostly of direct or modified quotations from many selected reports that present and evaluate methods for determining specific yield, limitations of those methods, and results of the determinations made on a wide variety of rock and soil materials. Although no particular values are recommended in this report, a table summarizes values of specific yield, and their averages, determined for 10 rock textures. The following is an abstract of the table.\n\n[Table]","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1662D","usgsCitation":"Johnson, A., 1967, Specific yield: compilation of specific yields for various materials: U.S. Geological Survey Water Supply Paper 1662, v, 74 p. :ill., maps ;23 cm., https://doi.org/10.3133/wsp1662D.","productDescription":"v, 74 p. :ill., maps ;23 cm.","costCenters":[],"links":[{"id":27352,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1662d/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137663,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1662d/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fc25c","contributors":{"authors":[{"text":"Johnson, A.I.","contributorId":82676,"corporation":false,"usgs":true,"family":"Johnson","given":"A.I.","email":"","affiliations":[],"preferred":false,"id":144465,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":22378,"text":"ofr677 - 1967 - Cinder Lake crater field location test","interactions":[],"lastModifiedDate":"2019-06-27T14:03:53","indexId":"ofr677","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"67-7","title":"Cinder Lake crater field location test","docAbstract":"<p>When the Apollo astronauts land on the Moon, their precise location will not be known. The real-time geologic mapping planned for the first mission could best be done if the exact position of the landing site were determined. The astronauts may have to find their position, with or without assistance from the Earth-based scientific mission center, before leaving the Lunar Module (LM), and the less time this takes, the more time will be available for exploring the lunar surface.</p><p>These considerations suggested the following questions: Could astronauts accurately locate themselves and how much time would it take?</p><p>The U.S. Geological Survey began studying this problem in July 1967. A crater field replica of a portion of the lunar surface was constructed and an LM mockup placed on it. Test subjects were asked to locate their exact position on a Lunar Orbiter photograph by comparing the photograph with the crater patterns visible through the LM windows. This \"curiosity\" test was part of a general survey of the problem and was intended to generate ideas that would enable intelligent planning of detailed tests if such tests become necessary. </p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr677","issn":"0094-9140","usgsCitation":"Bailey, N.G., 1967, Cinder Lake crater field location test: U.S. Geological Survey Open-File Report 67-7, iii, 15 p., https://doi.org/10.3133/ofr677.","productDescription":"iii, 15 p.","costCenters":[],"links":[{"id":155384,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1967/0007/report-thumb.jpg"},{"id":365119,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0007/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Arizona","otherGeospatial":"Cinder Lake","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -111.54315948486328,\n              35.297053740739855\n            ],\n            [\n              -111.48376464843749,\n              35.297053740739855\n            ],\n            [\n              -111.48376464843749,\n              35.33669357269044\n            ],\n            [\n              -111.54315948486328,\n              35.33669357269044\n            ],\n            [\n              -111.54315948486328,\n              35.297053740739855\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d8e4b07f02db5df924","contributors":{"authors":[{"text":"Bailey, Norman G.","contributorId":59439,"corporation":false,"usgs":true,"family":"Bailey","given":"Norman","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":188137,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":6263,"text":"pp567 - 1967 - Dictionary of Alaska place names","interactions":[],"lastModifiedDate":"2023-07-17T18:31:02.202386","indexId":"pp567","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"567","title":"Dictionary of Alaska place names","docAbstract":"<p>This work is an alphabetical list of the geographic names that are now applied and have been applied to places and features of the Alaska landscape. Principal names, compiled from modem maps and charts and printed in boldface type, generally reflect present-day local usage. They conform to the principles of the U.S. Board on Geographic Names for establishing standard names for use on Government maps and in other Government publications. Each name entry gives the present-day spelling along with variant spellings and names; identifies the feature named; presents the origin and history of the name; and, where possible, gives the meaning of an Eskimo, Aleut, Indian, or foreign name. Variant, obsolete, and doubtful names are alphabetically listed and are cross referenced, where necessary, to the principal entries. </p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp567","usgsCitation":"Orth, D., 1967, Dictionary of Alaska place names: U.S. Geological Survey Professional Paper 567, xi, 1,084 p., https://doi.org/10.3133/pp567.","productDescription":"xi, 1,084 p.","costCenters":[],"links":[{"id":139597,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0567/report-thumb.jpg"},{"id":419022,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0567/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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 \"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d9cf","contributors":{"authors":[{"text":"Orth, Donald J.","contributorId":8088,"corporation":false,"usgs":true,"family":"Orth","given":"Donald J.","affiliations":[],"preferred":false,"id":152403,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":2531,"text":"wsp1847 - 1967 - Ground water in the Eola-Amity Hills area, northern Willamette Valley, Oregon","interactions":[],"lastModifiedDate":"2017-02-03T13:42:56","indexId":"wsp1847","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1847","title":"Ground water in the Eola-Amity Hills area, northern Willamette Valley, Oregon","docAbstract":"The Eola-Amity Hills area ,comprises about 230 square miles on the west side of the Willamette Valley between Salem and McMinnville, Oreg. The area is largely rural, and agriculture is the principal occupation. \r\n\r\nRocks ranging in age from Eocene to Recent underlie the area. The oldest rocks are a sequence more than 5,000 feet thick of marine-deposited shale and siltstone strata, with thin interbeds of sandstone that range in age from Eocene to middle Oligocene. They are widely exposed in and west of the Eola-Amity Hills and underlie younger sedimentary and volcanic rocks throughout the study area. In the Eola-Amity Hills and Red Hills of Dundee, the Columbia River Group, a series of eastward-dipping basaltic lava flows locally of Miocene age, and conformably overlies the marine sedimentary rocks. The Columbia River Group ranges in thickness from less than 1 foot to about 900 feet and has an average thickness of about 200 feet. The formation is exposed in the Eola-Amity Hills and Red Hills of Dundee and, at places, extends to the east beneath younger rocks. \r\n\r\nOverlying the Columbia River Group and marine sedimentary rocks are nonmarine sedimentary deposits that range in thickness from less than 1 foot, where they lap up (to an altitude of about 200 ft) on the flanks of the higher hills, to several hundred feet along the east margin of the study area. These deposits include the Troutdale Formation of Pliocene age, the Willamette Silt of late Pleistocene age, and alluvium of the Willamette River and its tributaries. \r\n\r\nThe Troutdale Formation and the alluvium of the Willamette River contain the most productive aquifers in the Eola-Amity Hills area. These aquifers, which consist mainly of sand and gravel, generally yield moderate to large quantities of water to properly constructed wells. Basalt of the Columbia River Group yields small to moderate quantities of water to wells, and the marine sedimentary rocks and Willamette Silt generally yield small but adequate quantities of water for domestic and stock supplies. \r\n\r\nGround water from the Columbia River Group and nonmarine sedimentary rocks is chemically suitable for irrigation and other uses, as is the water from shallow depths in the marine sedimentary rocks. However, water from depths of more than several hundred feet in the marine sedimentary rocks contains large amounts of chloride and other dissolved mineral constitutents that make it unsuitable for most uses. Samples from three fairly closely spaced wells obtaining water from depth zones of 50 to 77, 191 to 201, and about 2,000 feet contained 172, 1,160, and 26,000 ppm (parts per million) of chloride, respectively. About 6,100 acre-feet of ground water was pumped from wells and withdrawn from springs for various uses during 1964; of this amount about 4,800 acre-feet was used for irrigation. The total volume of ground water withdrawn and put to beneficial use each year is small compared with the amount that discharges naturally by evapotranspiration and through undeveloped seeps and springs. Much of the natural discharge could be intercepted and put to beneficial use by pumping from wells. \r\n\r\nMajor problems affecting the development of ground water in the area include a) uneven areal distribution of permeable rocks, (b) undesirable chemical quality of the ground water locally in the marine sedimentary rocks, and (c) fine sand entering wells that tap the Troutdale Formation and thereby causing loss of well efficiency and costly wear on pumps and water-supply systems.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1847","usgsCitation":"Price, D., 1967, Ground water in the Eola-Amity Hills area, northern Willamette Valley, Oregon: U.S. Geological Survey Water Supply Paper 1847, iv, 66 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1847.","productDescription":"iv, 66 p. :ill., maps ;24 cm.","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":28756,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1847/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28757,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1847/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139103,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1847/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d9d1","contributors":{"authors":[{"text":"Price, Don","contributorId":30608,"corporation":false,"usgs":true,"family":"Price","given":"Don","email":"","affiliations":[],"preferred":false,"id":145355,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":2380,"text":"wsp1839K - 1967 - Ground-water resources of the Pascagoula River basin, Mississippi and Alabama","interactions":[],"lastModifiedDate":"2012-02-02T00:05:19","indexId":"wsp1839K","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1839","chapter":"K","title":"Ground-water resources of the Pascagoula River basin, Mississippi and Alabama","docAbstract":"Abundant ground-water resources underlie the Pascagoula River basin. These resources have been developed intensively in only a few places--namely, Hattiesburg, Laurel, Meridian, and Pascagoula. Seepage from the ground water reservoirs sustains the base flows of the Leaf, Chickasawhay, Pascagoula, and Escatawpa Rivers and their tributaries. \r\n\r\nThe fresh-water-bearing section is 300 to 3,500 feet thick and is composed chiefly of sand and clay of Eocene to Recent age. Major rock units represented are the Wilcox, Claiborne, Jackson, and Vicksburg Groups and formations of Miocene and Pliocene ages. \r\n\r\nAquifers in the Claiborne Group provide water for all purposes in the northern third of the basin. The Claiborne is underlain by the potentially important but virtually untapped Wilcox Group. Miocene aquifers are the main source of water supplies in the southern half of the basin, but Pliocene aquifers furnish most supplies in the Jackson County area at the basin's southern extremity. Much of the fresh-water section has undergone no water-supply development because of the great depth of many aquifers and the availability, at shallow depths, of supplies adequate for present needs. However, a large part of any substantial increase in ground-water withdrawal will probably come from wells deeper than those commonly drilled in the region. \r\n\r\nGround-water levels are within 50 feet of the surface in most places, and flowing wells are common in the valleys and near the coast. Water-level declines due to pumping have become serious problems only in a few localities of heavy withdrawal. In most of these places redistribution of pumpage would alleviate the problem of excessive drawdown. \r\n\r\nAlthough few wells in the basin yield more than 500 gallons per minute, yields of 2,000 gallons per minute or more could be reasonably expected from efficiently constructed wells almost anywhere in the region. \r\n\r\nTotal ground-water pumpage is estimated to be about 60 million gallons per day. Potential pumpage is many times that figure. Well fields capable of yielding several million gallons of water per day would be feasible in most places. The ground water is of good to excellent quality. Most of it is a sodium bicarbonate type of water. It usually is soft and has a low to moderate dissolved-solids content. Excessive iron is a problem in places, particularly where water supplies are obtained from shallow aquifers, but at least a part of the excess iron comes from corrosion of well and distribution-line fittings by slightly acidic water. \r\n\r\nSalt-water encroachment is a potential problem in the coastal area, but little increase in salinity has been observed in monitor wells in the period 1960-65. Saline-water resources are available for development at considerable depth in most of the region.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1839K","usgsCitation":"Newcome, R., 1967, Ground-water resources of the Pascagoula River basin, Mississippi and Alabama: U.S. Geological Survey Water Supply Paper 1839, iv, 36 p. :ill., maps ;24 cm., https://doi.org/10.3133/wsp1839K.","productDescription":"iv, 36 p. :ill., maps ;24 cm.","costCenters":[],"links":[{"id":137799,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1839k/report-thumb.jpg"},{"id":28339,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1839k/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a96e4b07f02db65a70d","contributors":{"authors":[{"text":"Newcome, Roy","contributorId":14796,"corporation":false,"usgs":true,"family":"Newcome","given":"Roy","affiliations":[],"preferred":false,"id":145109,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":1224,"text":"wsp1839M - 1967 - A comparison of methods of estimating potential evapotranspiration from climatological data in arid and subhumid environments","interactions":[],"lastModifiedDate":"2012-02-02T00:05:17","indexId":"wsp1839M","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1839","chapter":"M","title":"A comparison of methods of estimating potential evapotranspiration from climatological data in arid and subhumid environments","docAbstract":"This study compared potential evapotranspiration, computed from climatological data by each of six empirical methods, with pan evaporation adjusted to equivalent lake evaporation by regional coefficients. The six methods tested were the Thornthwaite, U.S. Weather Bureau (a modification of the Permian method), Lowry-Johnson, Blaney-Criddle, Lane, and Hamon methods. The test was limited to 25 sites in the arid and subhumid parts of Arizona, California, and Nevada, where pan evaporation and concurrent climatological data were available. However, some of the sites lacked complete climatological data for the application of all six methods. Average values of adjusted pan evaporation and computed potential evapotransp4ration were compared for two periods---the calendar year and the 6-month period from May 1 through October 31. \r\n\r\nThe 25 sites sampled a wide range of climatic conditions. Ten sites (group 1) were in a highly arid environment and four (group 2) were in an arid environment that was modified by extensive irrigation. The remaining 11 sites (group 3) were in a subhumid environment. \r\n\r\nOnly the Weather Bureau method gave estimates of potential evapotranspiration that closely agreed with the adjusted pan evaporation at all sites where the method was used. However, lack of climatological data restricted the use of the Weather Bureau method to seven sites. Results obtained by use of the Thornthwaite, Lowry-Johnson, and Hamon methods were consistently low. Results obtained by use of the Lane method agreed with adjusted pan evaporation at the group 1 sites but were consistently high at the group 2 and 3 sites. During the analysis it became apparent that adjusted pan evaporation in an arid environment (group 1 sites) was a spurious standard for evaluating the reliability of .the methods that were tested. Group 1 data were accordingly not considered when making conclusions as ,to which of the six methods tested was best. \r\n\r\nThe results of this study for group 2 and 3 data indicated that the Blaney-Criddle method, which uses climatological data that can be readily obtained or deduced, was the most practical of the six methods for estimating potential evapotranspiration. At all 15 sites in the two environments, potential evapotranspiration computed by the Blaney-Criddle method checked the adjusted pan evaporation within ?22 percent. This percentage range is generally considered to be the range of reliability for estimating lake evaporation from evaporation pans.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1839M","usgsCitation":"Cruff, R., and Thompson, T.H., 1967, A comparison of methods of estimating potential evapotranspiration from climatological data in arid and subhumid environments: U.S. Geological Survey Water Supply Paper 1839, iv, 28 p. :ill., map ;24 cm., https://doi.org/10.3133/wsp1839M.","productDescription":"iv, 28 p. :ill., map ;24 cm.","costCenters":[],"links":[{"id":137902,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1839m/report-thumb.jpg"},{"id":26140,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1839m/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b27e4b07f02db6b0f6a","contributors":{"authors":[{"text":"Cruff, R.W.","contributorId":77510,"corporation":false,"usgs":true,"family":"Cruff","given":"R.W.","email":"","affiliations":[],"preferred":false,"id":143398,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Thompson, T. H.","contributorId":23927,"corporation":false,"usgs":true,"family":"Thompson","given":"T.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143397,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":2232,"text":"wsp1835 - 1967 - Chemical quality of surface water in the Allegheny River basin, Pennsylvania and New York","interactions":[],"lastModifiedDate":"2017-06-21T11:05:53","indexId":"wsp1835","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1835","title":"Chemical quality of surface water in the Allegheny River basin, Pennsylvania and New York","docAbstract":"The Allegheny River is the principal source of water to many industries and to communities in the upper Ohio River Valley. The river and its many tributaries pass through 19 counties in northwestern and western Pennsylvania. The population in these counties exceeds 3 million. A major user of the Allegheny River is the city of Pittsburgh, which has a population greater than The Allegheny River is as basic to the economy of the upper Ohio River Valley in western Pennsylvania as are the rich deposits of bituminous coal, gas, and oil that underlie the drainage basin. During the past 5 years many streams that flow into the Allegheny have been low flowing because of droughts affecting much of the eastern United States. Consequently, the concentration of solutes in some streams has been unusually high because of wastes from coal mines and oil wells. These and other water-quality problems in the Allegheny River drainage basin are affecting the economic future of some areas in western Pennsylvania. \r\n\r\nBecause of environmental factors such as climate, geology, and land and water uses, surface-water quality varies considerably throughout the river basin. The natural quality of headwater streams, for example, is affected by saltwater wastes from petroleum production. One of the streams most affected is Kinzua Creek, which had 2,900 parts per million chloride in a sample taken at Westline on September 2, 1959. However, after such streams as the Conewango, Brokenstraw, Tionesta, Oil, and French Creeks merge with the Allegheny River, the dissolved-solids and chloride concentrations are reduced by dilution. Central segments of the main river receive water from the Clarion River, Redbank, Mahoning, and Crooked Creeks after they have crossed the coal fields of west-central Pennsylvania. At times, therefore, these streams carry coal-mine wastes that are acidic. The Kiskiminetas River, which crosses these coal fields, discharged sulfuric acid into the Allegheny at a rate of 299 tons a day during the 1962 water year (October 1, 1961, to September 30, 1962). Mine water affects the quality of the Allegheny River most noticeably in its lower part where large withdrawals are made by the Pittsburgh Water Company at Aspinwall and the Wilkinsburg-Penn Joint Water Authority at Nadine. At these places raw river water is chemically .treated in modern treatment plants to control such objectionable characteristics as acidity and excessive concentrations of iron and manganese.\r\n\r\nDissolved-solids content in the river varies along its entire length. In its upper reaches the water of the Allegheny River is a sodium chloride type, and at low flow, the sodium chloride is more than half the dissolved solids. In its lower reaches the water is a calcium sulfate .type, and at low flow the calcium sulfate is more than half the dissolved solids. In middle segments of the river from Franklin to Kittanning, water is more dilute and of a mixed type. Many small and several larger streams in the upper basin--such as the Conewango, Brokenstraw, Kinzua, Tionesta, and French Creeks--support large populations of game-fish. Even in segments of the Clarion River, Mahoning, and Redbank Creeks, which are at times affected by coal-mine wastes, fish are present. Although different species withstand varying amounts of contaminants in water, the continued presence of the fish indicates that the water is relatively pure and suitable for recreation and many other uses.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1835","usgsCitation":"McCarren, E.F., 1967, Chemical quality of surface water in the Allegheny River basin, Pennsylvania and New York: U.S. Geological Survey Water Supply Paper 1835, v, 74 p. :illus., maps (1 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/wsp1835.","productDescription":"v, 74 p. :illus., maps (1 fold. col. in pocket) ;24 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":27989,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1835/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27990,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1835/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137747,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1835/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dfe4b07f02db5e338a","contributors":{"authors":[{"text":"McCarren, Edward F.","contributorId":106472,"corporation":false,"usgs":true,"family":"McCarren","given":"Edward","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":144862,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":1112,"text":"wsp1836 - 1967 - Ground-water conditions and geologic reconnaissance of the Upper Sevier River basin, Utah","interactions":[],"lastModifiedDate":"2017-09-04T17:41:05","indexId":"wsp1836","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1836","title":"Ground-water conditions and geologic reconnaissance of the Upper Sevier River basin, Utah","docAbstract":"<p>The upper Sevier River basin is in south-central Utah and includes an area of about 2,400 .square miles of high plateaus and valleys. It comprises the entire Sevier River drainage basin above Kingston, including the East Fork Sevier River and its tributaries. The basin was investigated to determine general ground-water conditions, the interrelation of ground water and surface water, the effects of increasing the pumping of ground water, and the amount of ground water in storage.</p><p>The basin includes four main valleys - Panguitch Valley, Circle Valley, East Fork Valley, and Grass Valley - which are drained by the Sevier River, the East Fork Sevier River, and Otter Creek. The plateaus surrounding the valleys consist of sedimentary and igneous rocks that range in age from Triassic to Quaternary. The valley fill, which is predominantly alluvial gravel, sand, silt, and clay, has a maximum thickness of more than 800 feet.</p><p>The four main valleys constitute separate ground-water basins. East Fork Valley basin is divided into Emery Valley, Johns Valley, and Antimony subbasins, and Grass Valley basin is divided into Koosharem and Angle subbasins. Ground water occurs under both artesian and water-table conditions in all the basins and subbasins except Johns Valley, Emery Valley, and Angle subbasins, where water is only under water-table conditions. The water is under artesian pressure in beds of gravel and sand confined by overlying beds of silt and clay in the downstream parts of Panguitch Valley basin, Circle Valley basin, and Antimony subbasin, and in most of Koosharem subbasin. Along the sides and upstream ends of these basins, water is usually under water-table conditions.</p><p>About 1 million acre-feet of ground water that is readily available to wells is stored in the gravel and sand of the upper 200 feet of saturated valley fill. About 570,000 acre-feet is stored in Panguitch Valley basin, about 210,000 in Circle Valley basin, about 6,000 in Emery Valley subbasin, about 90,000 in Johns Valley subbasin, about 36,000 in Antimony subbasin, about 90,000 in Koosharem subbasin, and about 60,000 in Angle subbasin. Additional water, although it is not readily available to wells, is stored in beds of silt and clay. Some ground water also is available in the bedrock underlying and surrounding the basins, although the bedrock formations generally are poor aquifers.</p><p>The principal source of recharge to the valley fill in the upper Sevier River basin is infiltration from streams, canals, and irrigated fields. Some ground water also miles into the valley till from the bedrock surrounding the basins.</p><p>The basin contains about 300 wells, most of which are less than 4 inches in diameter, are less than 250 feet deep, and are used for domestic purposes and stock watering. More than half the wells are flowing wells in Koosharem subbasin.</p><p>Approximately 82,000 acre-feet of ground water was discharged in 1962 from the valley till. Springs discharged about 33,000 acre-feet, wells about 3,000, and drains about 3,000; and evapotranspiration from phreatophyte areas about 43,000 acre-feet. Springs in bedrock discharged an additional 75,000 acre-feet. Most of the water discharged by springs, wells, and drains was used for irrigation.</p><p>The ground water in the basin generally is of good chemical quality. The water is excellent for irrigation and stock but is not as desirable for most domestic and industrial uses because of its hardness. The dissolved-solids content of the ground water generally increases slightly from the upstream end of the individual ground-water basins to. the downstream end owing mostly to repeated use of the water for irrigation. <br></p><p>Surface water and ground water in the upper Sevier River basin are inter- connected, and the base flows of streams are affected by changes in ground- water levels. Increased pumping of ground water would result in (1) an increase in the recharge to the aquifers from surface-water sources or (2) a decrease in the discharge from streams, springs, flowing wells, and areas of phreatophytes or (3) a combination of these.</p><p>About 43,000 acre-feet of ground water is now discharged annually by evapotranspiration from phreatophyte areas, and perhaps one-third of this loss, or about 14,000 acre-feet, could be salvaged by eliminating wet areas and phreatophytes. The areas where water could be salvaged are at the downstream ends of Panguitch Valley basin, Circle Valley basin, and Antimony subbasin. Most of the 14,000 acre-feet 'of water could be pumped from large-diameter wells or developed by properly designed drains without greatly affecting stream- flow and with only moderate effect on 'spring discharge. If the wells were properly located, the pumping would lower water levels and dry up wet areas where phreatophytes grow. Conjunctive use of ground water and surface water would facilitate the more efficient use of all water resources in the basin</p>","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1836","collaboration":"Prepared in cooperation with the Utah State Engineer","usgsCitation":"Carpenter, C.H., Robinson, G., and Bjorklund, L.J., 1967, Ground-water conditions and geologic reconnaissance of the Upper Sevier River basin, Utah: U.S. Geological Survey Water Supply Paper 1836, Report: vi, 91 p.; 3 Plates: 35.00 in. x 49.87 in. or smaller, https://doi.org/10.3133/wsp1836.","productDescription":"Report: vi, 91 p.; 3 Plates: 35.00 in. x 49.87 in. or smaller","numberOfPages":"98","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":138011,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1836/report-thumb.jpg"},{"id":25869,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1836/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Reconnaissance geologic map and sections of the Upper Sevier River Basin, Utah"},{"id":25870,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1836/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing hydrologic data and phreatophyte areas in the Upper Sevier River Basin, Utah"},{"id":25871,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1836/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Graphs of water levels in selected wells and selected analyses of ground and surface water in the Upper Sevier River Basin, Utah"},{"id":25872,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1836/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","otherGeospatial":"Upper Sevier River Basin","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66d2be","contributors":{"authors":[{"text":"Carpenter, Carl H.","contributorId":46074,"corporation":false,"usgs":true,"family":"Carpenter","given":"Carl","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143197,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Robinson, Gerald B.","contributorId":46497,"corporation":false,"usgs":true,"family":"Robinson","given":"Gerald B.","affiliations":[],"preferred":false,"id":143198,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bjorklund, Louis Jay","contributorId":21138,"corporation":false,"usgs":true,"family":"Bjorklund","given":"Louis","email":"","middleInitial":"Jay","affiliations":[],"preferred":false,"id":143196,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":2768,"text":"wsp1829 - 1967 - Swatara Creek basin of southeastern Pennsylvania: An evaluation of its hydrologic system","interactions":[],"lastModifiedDate":"2022-05-11T18:58:56.606167","indexId":"wsp1829","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1829","title":"Swatara Creek basin of southeastern Pennsylvania: An evaluation of its hydrologic system","docAbstract":"<p>Local concentrations of population in the Swatara Creek basin of Pennsylvania find it necessary to store, transport, and treat water because local supplies are either deficient or have been contaminated by disposal of wastes in upstream areas. Water in the basin is available for the deficient areas and for dilution of the coal-mine drainage in the northern parts and the sewage wastes in the southern parts.</p>\n<p>Swatara Creek drains 576 square miles just east of Harrisburg, Pa., and is the largest tributary to the Susquehanna River from the north side below Harrisburg. It rises in the southern Pocono Mountains and flows southwestward across the Lebanon Plateau. On an average day Swatara Creek discharges more than 630 million gallons into the Susquehanna River at Middletown, Pa. In a year this amounts to about 23 inches of water over the entire basin and is the residual from an average annual precipitation of 45.5 inches. During an average year the flow in Swatara Creek from the upper third of the basin above Harper Tavern is always greater than 1,300 mgd (million gallons per day) for at least 15 days and is always greater than 25 mgd for at least 350 days. The daily streamflow from the basin averages 1.1 mgd per sq mi, but yields from different areas range from 0.97 to 1.22 mgd per sq mi. These variations are caused chiefly by differences in precipitation and land cover. The area of lowest yield is in the valleys west of Tremont, and the highest yields are in the Upper and Lower Little Swatara Creek subbasins.</p>\n<p>At high and medium stages the chemical character of the water in the streams is suitable for public and private supplies. At lower stages, defending on the areas and the amounts of contamination by coal-mine drainage and sewage pollution, the natural flow may require some treatment. At low stages the chemical characteristics of the natural flow not affected by man is almost identical with that of the ground water in the area drained by the stream. In general, the total dissolved solids range from about 25 to 400 parts per million and the hardness is as much as about 300 parts per million.</p>\n<p>The ground-water increment to the base flow of Swatara Creek averages about&nbsp;240 mgd, or about 8.8 inches annually, for the basin. Generally, ground-water&nbsp;supplies in amounts of less than 0.5 mgd can be developed south of Blue Mountain. Supplies of several million gallons per day have been developed for industrial use from the permeable limestones in the south-central part of the basin. More intensive investigation in other parts of the basin would indicate areas where supplies of more than 0.5 mgd could be developed from properly spaced wells. The chemical character of water from wells depends largely on the host rock. In highly soluble rocks water contains large amount of dissolved solids; in more resistant rocks concentrations are lower. The chemical character of unpolluted ground water generally reflects the composition of the more readily soluble minerals in the local geologic environment. Areas contaminated by septic- tank effluent may have above normal amounts of nitrate and detergent products. Except where polluted, most ground water is suitable for public and industrial uses without extensive treatment.</p>\n<p>Sites for storage of surface water exist in the part of the basin lying in the valley and ridge area. As much as 30 to 40 percent of the annual flow could be impounded for release as low-flow augmentation for dilution of mine drainage and other wastes in the basin. Low sediment yields of supplying drainage areas would ensure a long life expectancy of reservoirs at these sites.</p>\n<p>Overbank flooding of the main stem of the Swatara Creek and its tributaries has occurred many times in the past. However, it has not been a hazard because urban development has not encroached on the flood plain. An inundation map of the August 1933 flood provides a basis that urban planners may use to avoid future damage. As water in the Swatara Creek moves downstream to the Susquehanna River, the flow is influenced consecutively by a large annual rainfall on the northern valley and ridge area, the wastes of surface and subsurface coal-mining activities, and less annual rainfall on the part of the basin lying in the Lebanon Plateau area; the flow is supplemented and further influenced by many tributaries and by the industrial and domestic wastes that are carried by these secondary streams.</p>\n<p>The annual precipitation ranges from 52 inches at the east edge and 49 inches at the west edge of the mountainous part of the basin to about 41 inches at the southwestern part at Middletown. The rainfall generally is adequate during the growing season to mature the crops. The mean annual temperature at Lebanon is about 52&deg;F, and the growing season is about 180 days.</p>\n<p>In this report the basin has been divided into eight hydrologic zones, leased on runoff, natural use of water, and chemical character of water. Four zones lie in the valley and ridge area, three lie in the Lebanon Plateau area, and one lies in the highland along the southeastern basin boundary. In each of the zones the hydrologic characteristics are virtually the same, but they may be completely different from those in adjacent zones. The boundaries of the zones generally coincide with boundaries between geologic formations, and the areas in each zone include rocks of similar influence on water.</p>\n<p>Streams in zone 4 at the northeast edge of the plateau have the highest average surface runoff from 1.2 to 1.1 mgd per sq mi whereas those in zone 2 at the northwest edge of the valley and ridge area have the lowest, about 1.0 mgd. Streams in zone 8, along the southeast edge of the basin, have the largest sustained low-flow yield, about 0.26 to 0.19 mgd per sq mi; those in zone 5 overlying the Martinsburg Shale east of Harrisburg have the smallest sustained low-flow yields, 0.03 to 0.01 mgd. Streams in the limestone area of&nbsp;zone 7 have the greatest range in low-flow yields in any one zone from 0.60 to 0 mgd per sq mi. Low-flow yields in zones 1 through 4 range from 0.13 to 0.03 mgd per sq mi.</p>\n<p>Surface flows from zones 1 and 2 are generally acidic and contain high concentrations of sulfate, iron, and total dissolved solids especially where contaminated with mine wastes. Surface flows from zones 3 and 4 are dilute, slightly alkaline, and suitable for public water supplies. Surface flows from zones 5, 6, and 7 are alkaline and contain moderate concentrations of dissolved solids with waters of highest hardness occurring in zone 7. Surface flows from zone 8 are dilute to moderately mineralized and are relatively high in silica concentration. Nitrate concentrations are high in surf Fee flows below sewage outfalls and in ground water contaminated by septic tank effluent and industrial wastes.</p>\n<p>Average annual sediment yields of 550 to 650 tons per square mile are characteristic of zones 1 and 2 where strip mining has destroyed the forest cover and coal culm is carried into the streams. From agricultural lands on the Martinsburg Shale in zones 5 and 6, annual sediment yields range from 300 to 350 tons per square mile; but from agricultural lands on the siliceous rocks in zone 8 and zones 3 and 4 in the valley and ridge area, the sediment yield ranges from 200 to 250 tons annually per square mile. Lowest annual sediment yields in the basin are in the forested areas of siliceous rocks in zones 2, 3, 4, and 5, and in the sinkhole topography of the limestones in zone 7 where the yield ranges from 30 to 35 tons and 50 to 60 tons per square mile, respectively.</p>\n<p>The amount of ground water that can be developed in the basin is dependent on the ability of the underlying rocks to yield water to wells. More than 300 gpm (gallons per minute) can be obtained from wells in alluvial materials in the valley bottoms and in some of the limestones where large solution channels and fractures are penetrated by the wells. From 50 to 300 gpm can be obtained from wells in loosely cemented sandstones and in fractured limestones. From 10 to 50 gpm can be developed from wells in the shales and harder sandstones. The most dense rocks will yield from 1 to 10 gpm from fractures and crevices. Most wells yield water from the upper 350 feet of the formation, for this part contains the most fractures or solution channels.</p>\n<p>Studies show that the velocity at which a contaminant will move downstream in the basin is related to the discharge of the stream at the time. At a stream discharge of about 400 mgd at Pine Grove, a contaminant in Swatara Creek would require about 40 hours to move from Pine Grove to Middletown. As a result of dispersion and dilution, the maximum concentration of the contaminant at Middletown would be less than 20 percent the concentration at Pine Grove under these conditions.</p>\n<p>An evaluation of the availability of water in the basin indicates that about I,239 mgd enters as precipitation, 630 mgd leaves as streamflow, 580 mgd is evaporated and transpired, and 56 mgd is diverted for use by man. Not all the diversions for man's use are lost to the basin, as about 27 mgd is returned as sewage for reuse. About one-fourth of the waste water is returned to the ground and the remainder to stream drainageways. Of that diverted by man, 11.6 mgd is used for public supply and 44.4 mgd for industrial and private supplies. Diversions of streamflow furnish 86 percent of the public supply and&nbsp;27 percent of the industrial supply, and ground-water sources yield the remainder.</p>\n<p>Municipal and private sewage treatment plants are upgrading the waste water in many places, but no provisions are being made for treatment other than natural dilution and assimilation for the 15 mgd of coal-nine drainage in the northern part of the basin. Technology for economic treatment of mine water is not available at this time, although research in this field is being done.</p>\n<p>Urbanization eastward from Harrisburg and around Lebanon has increased the population density of the basin. Densities of 500 people per square mile and water use exceeding 2.0 mgd per sq mi can be expected in the future. By the year 2000 the population of the basin may increase 60 percent; and if the per capita rate of use increases 0.5 percent per year the domestic requirements for water will be about two times the present use, or 23 mgd. Similarly, if the present 1:4 ratio of domestic use to industrial use of water continues, at least 89 mgd will be needed for industry in the future. Although an increase to twice the present use of water can be foreseen, or 112 mgd, water for the dilution and assimilation of wastes from treatment systems are not included.</p>\n<p>Providing water for dilution of wastes from treatment plants has not been a problem, but in the future the amounts needed for this purpose will be greater as the population increases. As water becomes more valuable, treatment of sewage wastes to reduce the biochemical-oxygen-demand load by at least 80 to 90 percent will be necessary to conserve water for more productive uses. As much as 100 mgd may be needed for waste dilution in the basin by year 2000.</p>\n<p>The present trends in suburban and light industrial development will probably persist in the basin. Problems arising through changes in economic value of water, conflicts in use, and alternatives in development are typical of those confronting the manager of a water-resource system.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1829","usgsCitation":"Stuart, W.T., Schneider, W.J., and Crooks, J., 1967, Swatara Creek basin of southeastern Pennsylvania: An evaluation of its hydrologic system: U.S. Geological Survey Water Supply Paper 1829, Report: vii, 79 p.; 3 Plates: 37.50 x 44.76 inches or smaller, https://doi.org/10.3133/wsp1829.","productDescription":"Report: vii, 79 p.; 3 Plates: 37.50 x 44.76 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":29207,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1829/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":400539,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25034.htm"},{"id":29206,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1829/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 3"},{"id":29205,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1829/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":29204,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1829/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"},{"id":138606,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1829/report-thumb.jpg"}],"scale":"250000","country":"United States","state":"Pennsylvania","otherGeospatial":"Swatara Creek basin","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -76.809,\n              40.669\n            ],\n            [\n              -76.809,\n              40.178\n            ],\n            [\n              -76.19,\n              40.178\n            ],\n            [\n              -76.19,\n              40.669\n            ],\n            [\n              -76.809,\n              40.669\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db687ed9","contributors":{"authors":[{"text":"Stuart, Wilbur Tennant","contributorId":77513,"corporation":false,"usgs":true,"family":"Stuart","given":"Wilbur","email":"","middleInitial":"Tennant","affiliations":[],"preferred":false,"id":145752,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schneider, William J.","contributorId":47349,"corporation":false,"usgs":true,"family":"Schneider","given":"William","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145751,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Crooks, James W.","contributorId":46078,"corporation":false,"usgs":true,"family":"Crooks","given":"James W.","affiliations":[],"preferred":false,"id":145750,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":12950,"text":"ofr6743 - 1967 - Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque","interactions":[{"subject":{"id":12950,"text":"ofr6743 - 1967 - Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque","indexId":"ofr6743","publicationYear":"1967","noYear":false,"title":"Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque"},"predicate":"SUPERSEDED_BY","object":{"id":33960,"text":"b1272A - 1969 - Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque","indexId":"b1272A","publicationYear":"1969","noYear":false,"chapter":"A","title":"Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque"},"id":1}],"supersededBy":{"id":33960,"text":"b1272A - 1969 - Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque","indexId":"b1272A","publicationYear":"1969","noYear":false,"title":"Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque"},"lastModifiedDate":"2024-05-24T19:47:31.89876","indexId":"ofr6743","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"67-43","title":"Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque","docAbstract":"<p>Exploration for phosphate rock in Colombia was successfully carried out in 3 1/2 months by the U.S. Geological Survey and the Inventorio Minero of the Servicio Geologico Nacional, under the auspices of the U.S. Agency for International Development. A modern theory of exploration based on model studies of phosphorite deposits is that phosphate is deposited in the miogeosyncline adjacent to the foreland or craton, where parts of the ocean are deep, where deposition of clastic material is at a minimum, and where upwelling currents deposit a suite of rocks characterized by chert, black shale, carbonate rock, and phosphorite. Although phosphate is found in rocks of all geologic periods, economic deposits are known only in certain of: the periods--one of these being the Late Cretaceous.</p><p>As previous work had demonstrated that phosphate is present in Colombia only in rocks of Cretaceous age, and is most abundant in rocks of Late Cretaceous age--the La Luna Formations and Guadalupe--in the Cordillera Oriental, work was accordingly confined to the Cordillera Oriental and to rocks of Late Cretaceous age. Particular emphasis was paid to facies changes in the miogeosyncline; the field investigation pointed to the area in Norte de Santander where the best phosphorite was found. Phosphate deposits were found in both the geosynclinal and the platform facies in Upper Cretaceous rocks spread through a large area of the Cordillera Oriental, from Huila in the south to Norte de Santander in the north, a distance of more than 600 kilometers.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6743","usgsCitation":"Cathcart, J.B., Zambrano O., F., and Mojica G., P., 1967, Phosphate rock in Colombia - a preliminary report, with a section on the phosphate occurrence at Turmeque: U.S. Geological Survey Open-File Report 67-43, Report: vii, 124 p.; 3 Plates: 12.01 x 8.21 inches or smaller, https://doi.org/10.3133/ofr6743.","productDescription":"Report: vii, 124 p.; 3 Plates: 12.01 x 8.21 inches or smaller","costCenters":[],"links":[{"id":429276,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1967/0043/figure-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":429275,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1967/0043/figure-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":429274,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1967/0043/figure-II.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":429273,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0043/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":146695,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1967/0043/report-thumb.jpg"}],"country":"Columbia","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -77.91650781780235,\n              13.081466618213597\n            ],\n            [\n              -77.91650781780235,\n              -2.087789106482802\n            ],\n            [\n              -67.61083266704605,\n              -2.087789106482802\n            ],\n            [\n              -67.61083266704605,\n              13.081466618213597\n            ],\n            [\n              -77.91650781780235,\n              13.081466618213597\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adde4b07f02db686d48","contributors":{"authors":[{"text":"Cathcart, James Bachelder","contributorId":19540,"corporation":false,"usgs":true,"family":"Cathcart","given":"James","email":"","middleInitial":"Bachelder","affiliations":[],"preferred":false,"id":167019,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zambrano O., Francisco","contributorId":54606,"corporation":false,"usgs":true,"family":"Zambrano O.","given":"Francisco","email":"","affiliations":[],"preferred":false,"id":167020,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mojica G., Pedro","contributorId":67102,"corporation":false,"usgs":true,"family":"Mojica G.","given":"Pedro","email":"","affiliations":[],"preferred":false,"id":167021,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":52647,"text":"ofr67276 - 1967 - Electric analog model study of the hydrology of the Saginaw Formation in the Lansing, Michigan, area","interactions":[],"lastModifiedDate":"2012-02-02T00:11:25","indexId":"ofr67276","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"67-276","title":"Electric analog model study of the hydrology of the Saginaw Formation in the Lansing, Michigan, area","language":"ENGLISH","doi":"10.3133/ofr67276","usgsCitation":"Wheeler, M., 1967, Electric analog model study of the hydrology of the Saginaw Formation in the Lansing, Michigan, area: U.S. Geological Survey Open-File Report 67-276, 70 p., https://doi.org/10.3133/ofr67276.","productDescription":"70 p.","costCenters":[],"links":[{"id":178647,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a25e4b07f02db60edd5","contributors":{"authors":[{"text":"Wheeler, Merlin","contributorId":94736,"corporation":false,"usgs":true,"family":"Wheeler","given":"Merlin","email":"","affiliations":[],"preferred":false,"id":245699,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":55806,"text":"ofr67280 - 1967 - Analog-model study of the groundwater reservoir in the Santa Clara Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:12:17","indexId":"ofr67280","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"67-280","title":"Analog-model study of the groundwater reservoir in the Santa Clara Valley, California","language":"ENGLISH","doi":"10.3133/ofr67280","usgsCitation":"Wood, P., 1967, Analog-model study of the groundwater reservoir in the Santa Clara Valley, California: U.S. Geological Survey Open-File Report 67-280, 18 p.; 2 figs., https://doi.org/10.3133/ofr67280.","productDescription":"18 p.; 2 figs.","costCenters":[],"links":[{"id":184690,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db683a07","contributors":{"authors":[{"text":"Wood, P.R.","contributorId":102068,"corporation":false,"usgs":true,"family":"Wood","given":"P.R.","email":"","affiliations":[],"preferred":false,"id":254300,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":52625,"text":"ofr67199 - 1967 - Discovery of phosphate rock in Saudi Arabia and recommended program of further study","interactions":[],"lastModifiedDate":"2016-02-29T11:33:21","indexId":"ofr67199","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"67-199","title":"Discovery of phosphate rock in Saudi Arabia and recommended program of further study","docAbstract":"<p>In the period August 12, to September 3, 1965, I was assigned as a phosphate specialist to the U.S. Geological Survey Group in Saudi Arabia to work in cooperation with the Ministry of Petroleum and Mineral Resources of the Saudi Arabian Government. &nbsp;My assignment was to evaluate the phosphate potential of Saudi Arabia, train a Saudi Arabian geologist counterpart in modern techniques of phosphate exploration, and to help set up a program of exploration. &nbsp;These objectives have been largely fulfilled. &nbsp;In addition phosphate rock was discovered.</p>\n<p>&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr67199","usgsCitation":"Sheldon, R.P., 1967, Discovery of phosphate rock in Saudi Arabia and recommended program of further study: U.S. Geological Survey Open-File Report 67-199, 9 p., https://doi.org/10.3133/ofr67199.","productDescription":"9 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":177538,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr67199.jpg"},{"id":318178,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0199/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"Saudi Arabia","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[42.77933,16.34789],[42.64957,16.77464],[42.34799,17.07581],[42.27089,17.47472],[41.75438,17.83305],[41.22139,18.6716],[40.93934,19.48649],[40.24765,20.17463],[39.80168,20.33886],[39.1394,21.2919],[39.0237,21.98688],[39.06633,22.57966],[38.49277,23.68845],[38.02386,24.07869],[37.48363,24.28549],[37.15482,24.85848],[37.20949,25.08454],[36.93163,25.60296],[36.6396,25.82623],[36.24914,26.57014],[35.64018,27.37652],[35.13019,28.06335],[34.63234,28.05855],[34.78778,28.60743],[34.83222,28.95748],[34.95604,29.35655],[36.06894,29.19749],[36.50121,29.50525],[36.74053,29.86528],[37.50358,30.00378],[37.66812,30.33867],[37.99885,30.5085],[37.00217,31.50841],[39.00489,32.01022],[39.19547,32.16101],[40.39999,31.88999],[41.88998,31.19001],[44.7095,29.17889],[46.56871,29.09903],[47.45982,29.00252],[47.70885,28.52606],[48.41609,28.552],[48.80759,27.68963],[49.29955,27.46122],[49.47091,27.11],[50.15242,26.68966],[50.21294,26.27703],[50.1133,25.94397],[50.23986,25.60805],[50.52739,25.32781],[50.66056,24.9999],[50.81011,24.75474],[51.11242,24.55633],[51.38961,24.62739],[51.57952,24.2455],[51.61771,24.01422],[52.00073,23.00115],[55.0068,22.49695],[55.20834,22.70833],[55.66666,22],[54.99998,19.99999],[52.00001,19],[49.11667,18.61667],[48.18334,18.16667],[47.46669,17.11668],[47,16.95],[46.74999,17.28334],[46.36666,17.23332],[45.4,17.33334],[45.21665,17.43333],[44.06261,17.41036],[43.79152,17.31998],[43.38079,17.57999],[43.1158,17.08844],[43.21838,16.66689],[42.77933,16.34789]]]},\"properties\":{\"name\":\"Saudi Arabia\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64ab14","contributors":{"authors":[{"text":"Sheldon, Richard Porter","contributorId":59018,"corporation":false,"usgs":true,"family":"Sheldon","given":"Richard","email":"","middleInitial":"Porter","affiliations":[],"preferred":false,"id":245666,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":40723,"text":"ofr6711 - 1967 - Preliminary geologic section from Pahute Mesa, Nevada Test Site, to Enterprise, Utah","interactions":[],"lastModifiedDate":"2025-09-25T20:28:47.98929","indexId":"ofr6711","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"67-11","title":"Preliminary geologic section from Pahute Mesa, Nevada Test Site, to Enterprise, Utah","docAbstract":"The 154-mile long geologic cross section trends nearly perpendicular to the structural grain of the Basin-Range province in Nevada, and in Utah extends eastward into the transition zone between the Basin-Range and Colorado Plateau provinces. The structure is characterized by complex thrust: faults, involving uppermost Precambrian to lower Mesozoic sedimentary rocks, and normal faults which cut: the thick sequence of Tertiary volcanic rocks as well as older rocks. Some of the normal faults are the result of caldera collapse. The principal normal faults trend northerly west: of Delamar, Nev., and form north-trending basins and ranges. Farther east the principal faults trend northwesterly, and form a moderately rugged highland rather than distinct basins and ranges. \r\n\r\nThe uppermost Precambrian-Paleozoic strata thin markedly eastward across the region. The pre-Pennsylvanian sedimentary rocks vary from 32,500 feet: in thickness at the Nevada Test: Site (Harley Barnes, E. N. Hinrichs, F. A. McKeown and P. P. Orkild, written commun., 1963) to 4,500 feet: in the Beaver Dam Mountains in western Utah (Cook, 1960). Thick Mesozoic deposits, similar to those of the Colorado Plateau, are present in western Utah, but are represented in eastern Nevada by only thin patches of Triassic rock.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6711","usgsCitation":"Barosh, P., 1967, Preliminary geologic section from Pahute Mesa, Nevada Test Site, to Enterprise, Utah: U.S. Geological Survey Open-File Report 67-11, Report: 37 p.; 2 Plates: 45.51 × 18.82 inches and 19.54 × 35.74 inches, https://doi.org/10.3133/ofr6711.","productDescription":"Report: 37 p.; 2 Plates: 45.51 × 18.82 inches and 19.54 × 35.74 inches","costCenters":[],"links":[{"id":496182,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8157.htm","linkFileType":{"id":5,"text":"html"}},{"id":78000,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0011/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":77999,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1967/0011/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":77998,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1967/0011/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":171316,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1967/0011/report-thumb.jpg"}],"country":"United States","state":"Nevada, Utah","city":"Enterprise","otherGeospatial":"Nevada Test Site, Pahute Mesa","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -116.375,\n              37.583\n            ],\n            [\n              -116.375,\n              37.267\n            ],\n            [\n              -113.716,\n              37.267\n            ],\n            [\n              -113.716,\n              37.583\n            ],\n            [\n              -116.375,\n              37.583\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abce4b07f02db67369e","contributors":{"authors":[{"text":"Barosh, P. J.","contributorId":103347,"corporation":false,"usgs":true,"family":"Barosh","given":"P. J.","affiliations":[],"preferred":false,"id":223857,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":32595,"text":"32595 - 1967 - National Atlas, Indian tribes, cultures & languages","interactions":[],"lastModifiedDate":"2017-03-29T12:59:50","indexId":"32595","displayToPublicDate":"1991-01-01T09:59:44","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"title":"National Atlas, Indian tribes, cultures & languages","docAbstract":"<p>Tribal distributions depicted on these maps (and on all other tribal maps covering a comparable area) are arbitrary at many points. Detailed knowledge of tribal areas was acquired at different times in different regions. For example, by the time knowledge was gained of the areas occupied by Plains tribes, many groups in the East had become extinct or had moved from their aboriginal locations. Some of these movements ultimately affected distributions on the Plains prior to reasonably detailed knowledge of Plains occupancy. Hence, it is not possible to approximate aboriginal areas of occupancy on a single map of continental scope. Furthermore, most groups did not occupy sharply defined areas, so that the delineation of territories is misleading.</p><p>Distributions were derived, with slight modifications, from Indian tribes of North America (Driver and others, 1953), and boundaries within California were simplified after Languages, territories, and names of California Indian tribes (Heizer, 1966). According to the authors of these publications, the boundaries shown are those of the mid-17th century in the Southeast and the eastern part of the Northeast, the late 17th and early 18th centuries farther west in the Northeast, the late 18th and early 19th centuries in the Plains, the late 18th century in California, and the middle-to-late 19th century elsewhere. Even so, many compromises had to be made.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/32595","usgsCitation":"Sturtevant, W.C., 1967, National Atlas, Indian tribes, cultures & languages, 2 Plates: 13.85 x 18.01 inches and 27.81 x 18.54 inches, https://doi.org/10.3133/32595.","productDescription":"2 Plates: 13.85 x 18.01 inches and 27.81 x 18.54 inches","costCenters":[],"links":[{"id":289518,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":338480,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/32595/plate-1_back.pdf","text":"Back","size":"2.63 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate - Back"},{"id":338479,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/32595/plate-1_front.pdf","text":"Front","size":"6.24 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate - Front"}],"scale":"7500000","projection":"Albers Equal Area","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53bd12e4e4b00cbf31f72341","contributors":{"authors":[{"text":"Sturtevant, William C.","contributorId":60963,"corporation":false,"usgs":true,"family":"Sturtevant","given":"William","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":208752,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70214101,"text":"70214101 - 1967 - Compilation of hydrologic data Green Creek, Brazos River basin, Texas, 1967","interactions":[],"lastModifiedDate":"2024-09-13T13:26:07.152429","indexId":"70214101","displayToPublicDate":"1967-09-12T11:42:37","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Compilation of hydrologic data Green Creek, Brazos River basin, Texas, 1967","docAbstract":"<p>The U.S. Soil Conservation Service is actively engaged in the installation of flood and soil erosion reducing measures in Texas under the authority of \"The Flood Control Act of 1936 and 1944\" and \"Watershed Protection and Flood Prevention Act\" (Public Law 566), as amended. The Soil Conservation Service has found a total of 3,438 floodwater-retarding structures to be physically and economically feasible in Texas. As of September 30, 1967, 1,196 of these structures had been built.</p><p>This watershed-development program will have varying but important effects on the natural surface- and ground-water resources of river basins, especially where a large number of the floodwater-retarding structures are built. Basic hydrologic data under natural and developed conditions are needed to appraise the effects of the structures on the yield and mode of occurrence of runoff.</p><p>Hydrologic investigations of these small watersheds, both developed and undeveloped, were begun by the Geological Survey in 1951 and are now being made in 11 areas (fig. 1). These studies are being made in cooperation with the Texas Water Development Board, the Soil Conservation Service, the San Antonio River Authority, the city of Dallas and the Tarrant County Water Control and Improvement District No. 1. The 11 study areas were chosen to sample watersheds having different rainfall, topography, geology, and soils. In four of the study areas (North, Little Elm, Mukewater, and Pin Oak Creeks), streamflow and rainfall records were collected prior to construction of the floodwater-retarding structures, thus affording the opportunity for analyses of the conditions \"before and after\" development. Structures have now been built in three of these study areas. A summary of the development of the floodwater-retarding structures in each study area as of September 30, 1967, is shown in table 1.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/70214101","collaboration":"Prepared in cooperation with Texas Water Development Board and Soil Conservation Service","usgsCitation":"U.S. Geological Survey, 1967, Compilation of hydrologic data Green Creek, Brazos River basin, Texas, 1967: Open-File Report, iii, 34 p., https://doi.org/10.3133/70214101.","productDescription":"iii, 34 p.","costCenters":[],"links":[{"id":425045,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70214101/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":425044,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70214101/report-thumb.jpg"}],"country":"United 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,{"id":70221310,"text":"70221310 - 1967 - Plans of the U.S.Geological Survey, water resources division for research, investigations, and data collection in ground water","interactions":[],"lastModifiedDate":"2021-06-09T17:49:06.328407","indexId":"70221310","displayToPublicDate":"1967-04-01T12:45:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Plans of the U.S.Geological Survey, water resources division for research, investigations, and data collection in ground water","docAbstract":"<p><span>The&nbsp;</span>Geological<span>&nbsp;</span>Survey<span>&nbsp;has been the foremost agency&nbsp;</span>in<span>&nbsp;the&nbsp;</span>investigation<span>&nbsp;of&nbsp;</span>ground<span>‐</span>water<span>&nbsp;</span>resources<span>&nbsp;</span>in<span>&nbsp;the United States beginning about 1910. Most of the basic principles of modern&nbsp;</span>ground<span>‐</span>water<span>&nbsp;hydrology were developed&nbsp;</span>in<span>&nbsp;the&nbsp;</span>Survey<span>'</span>s<span>&nbsp;program of cooperative&nbsp;</span>investigations<span>. Use of&nbsp;</span>ground<span>&nbsp;</span>water<span>&nbsp;</span>in<span>&nbsp;the United States&nbsp;</span>in<span>&nbsp;1960 was about 17½ percent of all&nbsp;</span>water<span>&nbsp;uses, excluding&nbsp;</span>water<span>&nbsp;power. The use will probably increase, though at a decreasing rate. Although amount of use may level off, the need to know about it will not. While coordinating its activities with those of the Office of&nbsp;</span>Water<span>&nbsp;</span>Data<span>&nbsp;Coordination and the Office of&nbsp;</span>Water<span>&nbsp;</span>Resources<span>&nbsp;</span>Research<span>, the&nbsp;</span>Survey<span>&nbsp;expects to step up its work&nbsp;</span>in<span>&nbsp;all three areas of&nbsp;</span>data<span>&nbsp;</span>collection<span>,&nbsp;</span>investigations<span>, and&nbsp;</span>research<span>. However, there will be changes of emphasis.&nbsp;</span>Collection<span>&nbsp;of raw&nbsp;</span>data<span>&nbsp;will tend to stress key observation points, and more and more observation of temperature and quality, including contaminants.&nbsp;</span>Investigations<span>&nbsp;will be aimed at upgrading reconnaissance coverage to general coverage for most of the Nation. The areal basis will be stream drainage basins and special hydrologic terranes, rather than political units. There will be an increase&nbsp;</span>in<span>&nbsp;the preparation of analog models for representative&nbsp;</span>ground<span>‐</span>water<span>&nbsp;systems.&nbsp;</span>In<span>&nbsp;</span>research<span>, the problem‐oriented basis will continue. Stress will be on basic principles that pertain to artificial recharge, and the natural recharge and discharge of&nbsp;</span>ground<span>‐</span>water<span>&nbsp;reservoirs; and also on the application of geologic principles on a regional scale. These are critical elements&nbsp;</span>in<span>&nbsp;the management of surface‐</span>water<span>&nbsp;and&nbsp;</span>ground<span>‐</span>water<span>&nbsp;</span>resources<span>&nbsp;conjunctively&nbsp;</span>in<span>&nbsp;river basins.</span></p>","language":"English","publisher":"Wiley","doi":"10.1111/j.1745-6584.1967.tb01244.x","usgsCitation":"Upson, J., 1967, Plans of the U.S.Geological Survey, water resources division for research, investigations, and data collection in ground water: Groundwater, v. 5, no. 2, p. 13-19, https://doi.org/10.1111/j.1745-6584.1967.tb01244.x.","productDescription":"7 p.","startPage":"13","endPage":"19","costCenters":[],"links":[{"id":386357,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"5","issue":"2","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Upson, J. E.","contributorId":49342,"corporation":false,"usgs":true,"family":"Upson","given":"J. E.","affiliations":[],"preferred":false,"id":817287,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70221311,"text":"70221311 - 1967 - Plans of the U.S.Geological Survey, water resources division for research, investigations, and data collection in ground water","interactions":[],"lastModifiedDate":"2021-06-11T11:51:46.396788","indexId":"70221311","displayToPublicDate":"1967-04-01T12:45:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Plans of the U.S.Geological Survey, water resources division for research, investigations, and data collection in ground water","docAbstract":"<p><span>The&nbsp;</span>Geological<span>&nbsp;</span>Survey<span>&nbsp;has been the foremost agency&nbsp;</span>in<span>&nbsp;the&nbsp;</span>investigation<span>&nbsp;of&nbsp;</span>ground<span>‐</span>water<span>&nbsp;</span>resources<span>&nbsp;</span>in<span>&nbsp;the United States beginning about 1910. Most of the basic principles of modern&nbsp;</span>ground<span>‐</span>water<span>&nbsp;hydrology were developed&nbsp;</span>in<span>&nbsp;the&nbsp;</span>Survey<span>'</span>s<span>&nbsp;program of cooperative&nbsp;</span>investigations<span>. Use of&nbsp;</span>ground<span>&nbsp;</span>water<span>&nbsp;</span>in<span>&nbsp;the United States&nbsp;</span>in<span>&nbsp;1960 was about 17½ percent of all&nbsp;</span>water<span>&nbsp;uses, excluding&nbsp;</span>water<span>&nbsp;power. The use will probably increase, though at a decreasing rate. Although amount of use may level off, the need to know about it will not. While coordinating its activities with those of the Office of&nbsp;</span>Water<span>&nbsp;</span>Data<span>&nbsp;Coordination and the Office of&nbsp;</span>Water<span>&nbsp;</span>Resources<span>&nbsp;</span>Research<span>, the&nbsp;</span>Survey<span>&nbsp;expects to step up its work&nbsp;</span>in<span>&nbsp;all three areas of&nbsp;</span>data<span>&nbsp;</span>collection<span>,&nbsp;</span>investigations<span>, and&nbsp;</span>research<span>. However, there will be changes of emphasis.&nbsp;</span>Collection<span>&nbsp;of raw&nbsp;</span>data<span>&nbsp;will tend to stress key observation points, and more and more observation of temperature and quality, including contaminants.&nbsp;</span>Investigations<span>&nbsp;will be aimed at upgrading reconnaissance coverage to general coverage for most of the Nation. The areal basis will be stream drainage basins and special hydrologic terranes, rather than political units. There will be an increase&nbsp;</span>in<span>&nbsp;the preparation of analog models for representative&nbsp;</span>ground<span>‐</span>water<span>&nbsp;systems.&nbsp;</span>In<span>&nbsp;</span>research<span>, the problem‐oriented basis will continue. Stress will be on basic principles that pertain to artificial recharge, and the natural recharge and discharge of&nbsp;</span>ground<span>‐</span>water<span>&nbsp;reservoirs; and also on the application of geologic principles on a regional scale. These are critical elements&nbsp;</span>in<span>&nbsp;the management of surface‐</span>water<span>&nbsp;and&nbsp;</span>ground<span>‐</span>water<span>&nbsp;</span>resources<span>&nbsp;conjunctively&nbsp;</span>in<span>&nbsp;river basins.</span></p>","language":"English","publisher":"Wiley","doi":"10.1111/j.1745-6584.1967.tb01244.x","usgsCitation":"Upson, J., 1967, Plans of the U.S.Geological Survey, water resources division for research, investigations, and data collection in ground water: Groundwater, v. 5, no. 2, p. 13-19, https://doi.org/10.1111/j.1745-6584.1967.tb01244.x.","productDescription":"7 p.","startPage":"13","endPage":"19","costCenters":[],"links":[{"id":386408,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"5","issue":"2","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Upson, J. E.","contributorId":49342,"corporation":false,"usgs":true,"family":"Upson","given":"J. E.","affiliations":[],"preferred":false,"id":817408,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70221309,"text":"70221309 - 1967 - An electrical analog study of the geometry of limestone solution","interactions":[],"lastModifiedDate":"2021-06-09T17:42:25.755466","indexId":"70221309","displayToPublicDate":"1967-01-01T12:38:36","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"An electrical analog study of the geometry of limestone solution","docAbstract":"<p><span>This&nbsp;</span>study<span>&nbsp;of the&nbsp;</span>geometry<span>&nbsp;of&nbsp;</span>limestone<span>&nbsp;</span>solution<span>&nbsp;is based on the following conditions: (1) the&nbsp;</span>limestone<span>&nbsp;is impermeable but contains and transmits water in joints, fractures, bedding‐plane partings, and&nbsp;</span>solution<span>&nbsp;channels; (2) at depth, the&nbsp;</span>limestone<span>&nbsp;aquifer is underlain by impermeable rock; (3) ground water in the&nbsp;</span>limestone<span>&nbsp;is under water‐table conditions; (4) recharge to the&nbsp;</span>limestone<span>&nbsp;is by infiltration of precipitation through the overlying rock to the zone of saturation; (5) discharge from the aquifer is by seeps and springs; and (6) ground water dissolves the&nbsp;</span>limestone<span>&nbsp;through which it flows, continuously modifying the flow pattern and the hydrologic properties of the medium. These conditions commonly are found in&nbsp;</span>limestone<span>&nbsp;terranes in the eastern and central United States. An&nbsp;</span>electrical<span>&nbsp;</span>analog<span>&nbsp;was constructed conforming to this description of the ground‐water flow system and has been used to define the pattern, velocity, and density of ground‐water flow and the relative length of time of contact of water with the aquifer. Successive models are used to illustrate progressive&nbsp;</span>limestone<span>&nbsp;</span>solution<span>&nbsp;and changes in ground‐water flow in the aquifer. The initial&nbsp;</span>analog<span>&nbsp;indicates a strongly convex water table with the greatest density of flow at shallow depths beneath the water table near the point of discharge. Successive models indicate greater concentration of flow near and on the level of ground‐water discharge, an overall lowering of the water table, and a pronounced flattening of the water table near the discharge point. Results of the&nbsp;</span>analog<span>&nbsp;</span>study<span>&nbsp;support the following conclusions: (1) The most active zone of&nbsp;</span>solution<span>&nbsp;is at shallow depths beneath the water table and near the point of ground‐water discharge. Consequently, the size of channels generally decreases with depth and increases with proximity to the point of ground‐water discharge. (2) Generally,&nbsp;</span>solution<span>&nbsp;channels have a greater lateral than vertical extent.</span></p>","language":"English","publisher":"Wiley","doi":"10.1111/j.1745-6584.1967.tb01235.x","usgsCitation":"Bedinger, M.S., 1967, An electrical analog study of the geometry of limestone solution: Groundwater, v. 59, no. 12, p. 24-24, https://doi.org/10.1111/j.1745-6584.1967.tb01235.x.","productDescription":"1 p.","startPage":"24","endPage":"24","costCenters":[],"links":[{"id":386356,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"59","issue":"12","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Bedinger, M. S.","contributorId":65452,"corporation":false,"usgs":true,"family":"Bedinger","given":"M.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":817286,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70210849,"text":"70210849 - 1967 - Scapolite in the Belt Series in the St. Joe-Clearwater Region, Idaho","interactions":[],"lastModifiedDate":"2020-06-29T16:42:29.404119","indexId":"70210849","displayToPublicDate":"1967-01-01T11:35:53","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1727,"text":"GSA Special Papers","active":true,"publicationSubtype":{"id":10}},"title":"Scapolite in the Belt Series in the St. Joe-Clearwater Region, Idaho","docAbstract":"<p>S<span class=\"small-caps\">capolite</span><span>&nbsp;</span>is a common rock-forming mineral in parts of the Belt Series of Precambrian age in southern Shoshone County and adjoining parts of Clearwater County, Idaho. It is most abundant in moderately metamorphosed calcareous shaly layers of the Wallace Formation but occurs also in their highly metamorphosed equivalents and in the lowest part of the Prichard Formation.</p><p>The mode of occurrence varies with distance from the Idaho batholith, with bulk composition, and with grade of metamorphism. In the northern part of the area where rocks were metamorphosed to the epidote-amphibolite facies, the highest concentration of scapolite is in layers rich in calcite, biotite, or hornblende and diopside. In biotite-rich layers interbedded with quartzite, scapolite is in round holoblasts; in carbonate granofels, crystals are euhedral to subhedral; and in hornblende- and diopside-bearing layers, small anhedral grains are common. In rocks metamorphosed to the amphibolite facies, such as diopside gneiss and calcium-magnesium-aluminum silicate rocks (here named “camalsite”), scapolite occurs in small anhedral grains. In diopside gneiss, scapolite is in thin layers that extend long distances parallel to the bedding. In camalsite, small masses exceptionally rich in scapolite are common.</p><p>The mode of occurrence and the distribution parallel to the bedding suggest that scapolite crystallized from a sedimentary rock that contained saline minerals. The scapolite contains much Cl but only a little SO<sub>3</sub>, suggesting that halite was the chief source mineral. The local high concentrations of scapolite occur in a zone where elements have been redistributed, either because of metamorphism of dispersed or layered saline minerals with accompanying migration of chlorine or because of metamorphism of primary local masses of such minerals.</p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/SPE86-p1","usgsCitation":"Hietanen, A., 1967, Scapolite in the Belt Series in the St. Joe-Clearwater Region, Idaho: GSA Special Papers, v. 86, p. 1-54, https://doi.org/10.1130/SPE86-p1.","productDescription":"54 p.","startPage":"1","endPage":"54","costCenters":[],"links":[{"id":375984,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho","otherGeospatial":"St. Joe-Clearwater region","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -116.83959960937499,\n              46.210249600187225\n            ],\n            [\n              -114.334716796875,\n              46.210249600187225\n            ],\n            [\n              -114.334716796875,\n              47.502358951968574\n            ],\n            [\n              -116.83959960937499,\n              47.502358951968574\n            ],\n            [\n              -116.83959960937499,\n              46.210249600187225\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"86","noUsgsAuthors":false,"publicationDate":"1967-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hietanen, Anna","contributorId":43841,"corporation":false,"usgs":true,"family":"Hietanen","given":"Anna","affiliations":[],"preferred":false,"id":791704,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70010564,"text":"70010564 - 1967 - Precision measurement of lead isotopes ratios: preliminary analyses from the U.S. mine, Bingham Canyon, Utah","interactions":[],"lastModifiedDate":"2023-12-13T13:18:38.53336","indexId":"70010564","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1427,"text":"Earth and Planetary Science Letters","active":true,"publicationSubtype":{"id":10}},"title":"Precision measurement of lead isotopes ratios: preliminary analyses from the U.S. mine, Bingham Canyon, Utah","docAbstract":"<div id=\"abstracts\" class=\"Abstracts u-font-serif text-s\"><div id=\"ab1\" class=\"abstract author\" lang=\"en\"><div id=\"aep-abstract-sec-id8\"><p>A gas-source mass spectrometer has been constructed for the precise measurement of lead isotope ratios. Sixteen analyses on 4 different preparations of the same galena made over a period of 2 months gave 95% confidence limits (per analysis) of<span>&nbsp;</span><i><sup>206</sup>Pb/<sup>204</sup>Pb= 0.080%,<span>&nbsp;</span><sup>207</sup>Pb/<sup>206</sup>Pb= 0.042%and<sup>208</sup>Pb/<sup>206</sup>Pb= 0.046%</i>.</p><p>Eight samples from the U.S. mine in the Bingham district have a linear relationship over the 1% range of their<sup>206</sup>Pb/<sup>204</sup>Pb ratios. The simplest model fitting these data suggests that the lead was separated from a primary system<span>&nbsp;</span><i>(μ=8.98) 1630±150m.y.</i><span>&nbsp;</span>ago and subsequently mixed with a radiogenic lead of similar age; biotite K-Ar dates for altered intrusive rocks associated with the ores provide an apparent age of mineralization and suggest that isotopic evolution of the lead was terminated about 36 m.y. ago.</p></div></div></div>","language":"English","publisher":"Elsevier","doi":"10.1016/0012-821X(67)90195-1","issn":"0012821X","usgsCitation":"Stacey, J.S., Moore, W.J., and Rubright, R., 1967, Precision measurement of lead isotopes ratios: preliminary analyses from the U.S. mine, Bingham Canyon, Utah: Earth and Planetary Science Letters, v. 2, no. 5, p. 489-499, https://doi.org/10.1016/0012-821X(67)90195-1.","productDescription":"11 p.","startPage":"489","endPage":"499","numberOfPages":"11","costCenters":[],"links":[{"id":218966,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Utah","otherGeospatial":"Bingham Canyon","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -112.3599157983052,\n              40.61550688525992\n            ],\n            [\n              -112.3599157983052,\n              40.21250278039901\n            ],\n            [\n              -111.85271775878975,\n              40.21250278039901\n            ],\n            [\n              -111.85271775878975,\n              40.61550688525992\n            ],\n            [\n              -112.3599157983052,\n              40.61550688525992\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"2","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a8141e4b0c8380cd7b424","contributors":{"authors":[{"text":"Stacey, J. S.","contributorId":72785,"corporation":false,"usgs":true,"family":"Stacey","given":"J.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":359178,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moore, W. J.","contributorId":84334,"corporation":false,"usgs":true,"family":"Moore","given":"W.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359179,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rubright, R.D.","contributorId":88871,"corporation":false,"usgs":true,"family":"Rubright","given":"R.D.","email":"","affiliations":[],"preferred":false,"id":359180,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70011549,"text":"70011549 - 1967 - Theory of friction based on brittle fracture","interactions":[],"lastModifiedDate":"2020-11-24T21:35:31.108544","indexId":"70011549","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2171,"text":"Journal of Applied Physics","active":true,"publicationSubtype":{"id":10}},"title":"Theory of friction based on brittle fracture","docAbstract":"<div class=\"hlFld-Abstract\"><div class=\"NLM_paragraph\">A theory of<span>&nbsp;</span>friction<span>&nbsp;</span>is presented that may be more applicable to<span>&nbsp;</span>geologic<span>&nbsp;</span>materials<span>&nbsp;</span>than the classic Bowden and Tabor theory. In the model, surfaces touch at the peaks of asperities and sliding occurs when the asperities fail by<span>&nbsp;</span>brittle<span>&nbsp;</span>fracture.<span>&nbsp;</span>The coefficient of<span>&nbsp;</span>friction,<span>&nbsp;</span>μ, was calculated from the strength of asperities of certain ideal shapes; for cone‐shaped asperities, μ is about 0.1 and for wedge‐shaped asperities, μ is about 0.15. For actual situations which seem close to the ideal model, observed μ was found to be very close to 0.1, even for<span>&nbsp;</span>materials<span>&nbsp;</span>such as<span>&nbsp;</span>quartz<span>&nbsp;</span>and calcite with widely differing strengths. If surface forces are present, the theory predicts that μ should decrease with load and that it should be higher in a vacuum than in air. In the presence of a fluid film between sliding surfaces, μ should depend on the area of the surfaces in contact. Both effects are observed. The character of wear particles produced during sliding and the way in which μ depends on normal load, roughness, and environment lend further support to the model of<span>&nbsp;</span>friction<span>&nbsp;</span>presented here.</div></div>","language":"English","publisher":"AIP","doi":"10.1063/1.1710026","issn":"00214922","usgsCitation":"Byerlee, J., 1967, Theory of friction based on brittle fracture: Journal of Applied Physics, v. 38, no. 7, p. 2928-2934, https://doi.org/10.1063/1.1710026.","productDescription":"7 p.","startPage":"2928","endPage":"2934","numberOfPages":"7","costCenters":[],"links":[{"id":220981,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"38","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb203e4b08c986b32554b","contributors":{"authors":[{"text":"Byerlee, J.D.","contributorId":69982,"corporation":false,"usgs":true,"family":"Byerlee","given":"J.D.","affiliations":[],"preferred":false,"id":361373,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
]}