{"pageNumber":"407","pageRowStart":"10150","pageSize":"25","recordCount":11004,"records":[{"id":1151,"text":"wsp1843 - 1967 - Geology and ground-water resources of the Big Sandy Creek Valley, Lincoln, Cheyenne, and Kiowa Counties, Colorado","interactions":[],"lastModifiedDate":"2022-02-02T19:11:07.313002","indexId":"wsp1843","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":"1843","title":"Geology and ground-water resources of the Big Sandy Creek Valley, Lincoln, Cheyenne, and Kiowa Counties, Colorado","docAbstract":"This report describes the geology and ground-water resources of that part of the Big Sandy Creek valley from about 6 miles east of Limon, Colo., downstream to the Kiowa County and Prowers County line, an area of about 1,400 square miles. The valley is drained by Big Sandy Creek and its principal tributary, Rush Creek. The land surface ranges from flat to rolling; the most irregular topography is in the sandhills south and west of Big Sandy Creek. Farming and livestock raising are the principal occupations. Irrigated lands constitute only a sin311 part of the project area, but during the last 15 years irrigation has expanded. \r\n\r\nExposed rocks range in age from Late Cretaceous to Recent. They comprise the Carlile Shale, Niobrara Formations, Pierre Shale (all Late Cretaceous), upland deposits (Pleistocene), valley-fill deposits (Pleistocene and Recent), and dune sand (Pleistocene and Recent). Because the Upper Cretaceous formations are relatively impermeable and inhibit water movement, they allow ground water to accumul3te in the overlying unconsolidated Pleistocene and Recent deposits. The valley-fill deposits constitute the major aquifer and yield as much as 800 gpm (gallons per mixture) to wells along Big Sandy and Rush Creeks. Transmissibilities average about 45,000 gallons per day per foot. Maximum well yields in the tributary valleys are about 200 gpm and average 5 to 10 gpm. The dune sand and upland deposits generally are drained and yield water to wells in only a few places. \r\n\r\nThe ground-water reservoir is recharged only from direct infiltration of precipitation, which annually averages about 12 inches for the entire basin, and from infiltration of floodwater. Floods in the ephemeral Big Sandy Creek are a major source of recharge to ground-water reservoirs. Observations of a flood near Kit Carson indicated that about 3 acre-feet of runoff percolated into the ground-water reservoir through each acre of the wetted stream channel The downstream decrease in channel and flood-plain width indicates that floodflows percolate to the ground-water reservoir. \r\n\r\nIn the project area at least 94,000 acre-feet of water is evaporated and transpired from the valley fill along Big Sandy Creek, 1,500 acre-feet is pumped, 250 acre-feet leaves the area as underflow, and 10,000 acre-feet leaves as surface flow. Surface-water irrigation has been unsuccessful because of the failure of diversion dams and because of excessive seepage from reservoirs.\r\n\r\nGround-water irrigation dates from about World War I; most of the 30 irrigation wells now in use, however, were drilled after 1937. Iv 1960 less than 1,000 acre-feet of water was pumped for irrigation, about 500 acre-feet was pumped for municipal use, and less than 10 acre-feet was pumped for rural use (stock and domestic). \r\n\r\nAlthough additional water is available in the valley-fill deposits of Big Sandy and Rush Creeks, large-scale irrigation probably will not develop in the immediate future; soils are unsuitable for crops in many places, and large water supplies are not available from individual wells. \r\nThe dissolved-solids content of the ground water in the valley-fill deposits \r\nranges from 507 to 5,420 parts per million. In the Big Sandy Creek valley the \r\ndissolved-solids content generally increases downstream, whereas in the Rush \r\nCreek valley the dissolved-solids content decreases downstream. Ground water \r\nin the Big Sandy Creek valley is suitable for most uses.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1843","usgsCitation":"Coffin, D.L., and Horr, C.A., 1967, Geology and ground-water resources of the Big Sandy Creek Valley, Lincoln, Cheyenne, and Kiowa Counties, Colorado: U.S. Geological Survey Water Supply Paper 1843, Report: iv, 49 p.; 1 Plate: 35.00 × 39.00 inches, https://doi.org/10.3133/wsp1843.","productDescription":"Report: iv, 49 p.; 1 Plate: 35.00 × 39.00 inches","costCenters":[],"links":[{"id":395290,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25059.htm"},{"id":25951,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1843/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25950,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1843/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137287,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1843/report-thumb.jpg"}],"country":"United States","state":"Colorado","county":"Cheyenne County, Kiowa County, Lincoln County","otherGeospatial":"Big Sandy Creek valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.6,\n 38.267\n ],\n [\n -102.4,\n 38.267\n ],\n [\n -102.4,\n 39.2820\n ],\n [\n -103.6,\n 39.2820\n ],\n [\n -103.6,\n 38.267\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db685807","contributors":{"authors":[{"text":"Coffin, Donald L.","contributorId":90696,"corporation":false,"usgs":true,"family":"Coffin","given":"Donald","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":143265,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Horr, Clarence Albert","contributorId":60611,"corporation":false,"usgs":true,"family":"Horr","given":"Clarence","email":"","middleInitial":"Albert","affiliations":[],"preferred":false,"id":143264,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":41366,"text":"ofr67112 - 1967 - Photogeologic map of the east half of the Laguna 4 quadrangle Bernalillo, Sandoval, and Valencia Counties, New Mexico","interactions":[],"lastModifiedDate":"2022-02-07T19:53:12.878467","indexId":"ofr67112","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":"67-112","title":"Photogeologic map of the east half of the Laguna 4 quadrangle Bernalillo, Sandoval, and Valencia Counties, New Mexico","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr67112","usgsCitation":"Hemphill, W.R., 1967, Photogeologic map of the east half of the Laguna 4 quadrangle Bernalillo, Sandoval, and Valencia Counties, New Mexico: U.S. Geological Survey Open-File Report 67-112, 1 Plate: 14.68 × 25.96 inches, https://doi.org/10.3133/ofr67112.","productDescription":"1 Plate: 14.68 × 25.96 inches","costCenters":[],"links":[{"id":172941,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":79120,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1967/0112/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":106381,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8152.htm","linkFileType":{"id":5,"text":"html"},"description":"8152"}],"scale":"62500","country":"United States","state":"New Mexico","county":"Bernalillo County, Sandoval County, Valencia County","otherGeospatial":"Laguna 4 quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -107.25,\n 35\n ],\n [\n -107,\n 35\n ],\n [\n -107,\n 35.25\n ],\n [\n -107.25,\n 35.25\n ],\n [\n -107.25,\n 35\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db686338","contributors":{"authors":[{"text":"Hemphill, W. R.","contributorId":19525,"corporation":false,"usgs":true,"family":"Hemphill","given":"W.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":224902,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2984,"text":"wsp1842 - 1967 - Water resources of the Marquette Iron Range area, Michigan","interactions":[],"lastModifiedDate":"2017-02-06T15:26:08","indexId":"wsp1842","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":"1842","title":"Water resources of the Marquette Iron Range area, Michigan","docAbstract":"

Large quantities of water are needed in the beneficiation and pelletizing processes by which the ore mined from low-grade iron-formations is upgraded into an excellent raw material for the iron and steel industry. Extensive reserves of low-grade iron-formation available for development herald an intensification of the demands upon the area's water supplies. This study was designed to provide water facts for public and private agencies in planning orderly development and in guiding the management of the water resources to meet existing and new requirements.

Inland lakes and streams are the best potential sources of water for immediate development. The natural flow available for 90 percent of the time in the Middle and East Branches of the Escanaba River, the Carp River, and the Michigamme River is about 190 cubic feet per second. Potential storage sites are identified, and their complete development could increase the available supply from the above streams to about 450 cubic feet per second.

Outwash deposits are the best potential sources of ground water. Large supplies could be developed from extensive outwash deposits in the eastern part of the area adjacent to Goose Lake Outlet and the East Branch Escanaba River. Other areas of outwash occur in the vicinity of Humboldt, West Branch Creek, and along the stream valleys. Streamflow data were used to make rough approximations of the ground-water potential in some areas. In general, however, the available data were not sufficient to permit quantitative evaluation of the potential ground-water supplies.

Chemical quality of the surface and ground waters of the area is generally acceptable for most uses. Suspended sediment in the form of mineral tailings in effluents from ore-processing plants is a potential problem. Existing plants use settling basins to effectively remove most of the suspended material. Available records indicate that suspended-sediment concentrations and loads in the receiving waters have not been significantly increased by these operations.

Present water use is about 60 cubic feet per second in the area. Thus, available water supplies are believed to be adequate for existing and foreseeable new uses. Water management, rather than water availability, is of prime consideration in this area. Time distribution of available water supplies, distribution of water to points of use, effect of surface-water development upon ground water and vice versa, and possible conflicts with competing uses are some of the management problems that are discussed. The presence of many inland lakes, favorable storage sites on streams, and several promising acquifers provide flexibility in possible water-management operations. A discussion of the interrelationships between surface and ground water and a ground-water budget are presented to render a better understanding of the hydrologic system with which water management will be concerned.

","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1842","collaboration":"Prepared in cooperation with the State of Michigan","usgsCitation":"Wiitala, S.W., Newport, T.G., and Skinner, E.L., 1967, Water resources of the Marquette Iron Range area, Michigan: U.S. Geological Survey Water Supply Paper 1842, Document: ix, 142 p.; 4 Plates: 30.00 x 20.25 inches or smaller, https://doi.org/10.3133/wsp1842.","productDescription":"Document: ix, 142 p.; 4 Plates: 30.00 x 20.25 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":139432,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1842/report-thumb.jpg"},{"id":29750,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1842/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29751,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1842/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29752,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1842/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29753,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1842/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29754,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1842/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Michigan","otherGeospatial":"Marquette Iron Range area","geographicExtents":"{ 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Gwyn","contributorId":39353,"corporation":false,"usgs":true,"family":"Newport","given":"Thomas","email":"","middleInitial":"Gwyn","affiliations":[],"preferred":false,"id":146101,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Skinner, Earl L.","contributorId":73191,"corporation":false,"usgs":true,"family":"Skinner","given":"Earl","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":146102,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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":"

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. 

","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":3775,"text":"cir537 - 1967 - Effects of the Truckee, California, earthquake of September 12, 1966","interactions":[],"lastModifiedDate":"2017-04-25T14:01:45","indexId":"cir537","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"537","title":"Effects of the Truckee, California, earthquake of September 12, 1966","docAbstract":"

The Truckee, Calif., earthquake of September 12, 1966, had a magnitude of 5.4 on the Richter scale, as reported by the U.S. Coast and Geodetic Survey. It was felt over an area extending from San Francisco eastward to Salt Lake City and from Bakersfield northward beyond Chico, Calif. Ground breakage due to seismic shaking occurred in unconsolidated alluvium along a zone about 10 miles long that trends about N. 30° E. and extends from a point west of Prosser Reservoir, 4 miles northeast of Truckee, to Hoke Valley. The concentration of ground breakage along this zone suggests that it may be related to a subsurface northeastward-trending fault rather than to buried extensions of the northwestward-trending faults that dominate the regional geologic structure.

Other effects of the earthquake include the following: (1) Damage to Prosser and Boca Dams, (2) minor damage to several bridges on Interstate Highway 80, (3) several earthquake-generated slumps or landslides on Interstate Highway 80 between Boca Dam and the California-Nevada boundary, (4) damage to the caretaker's house at Boca Dam and a lumber shed at Loyalton, (5) damage by falling rocks to the Farad powerhouse, to the wooden flume which supplies water to the powerhouse, and to the Southern Pacific Lines in Truckee Canyon, (6) minor damage to water wells and water distribution systems, particularly at Truckee, and (7) rejuvenation of springs throughout the Truckee-Russel Valley area.


","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir537","usgsCitation":"Kachadoorian, R., Yerkes, R.F., and Waananen, A.O., 1967, Effects of the Truckee, California, earthquake of September 12, 1966: U.S. Geological Survey Circular 537, Report: iii, 14 p.; Plate: 18.51 x 18.09 inches, https://doi.org/10.3133/cir537.","productDescription":"Report: iii, 14 p.; Plate: 18.51 x 18.09 inches","costCenters":[],"links":[{"id":30846,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1967/0537/report.pdf","text":"Report","size":"4.46 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":116995,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1967/0537/report-thumb.jpg"},{"id":340286,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/1967/0537/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Arizona, California, Idaho, Nevada, Oregon, Utah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.18945312500001,\n 44.731125592643274\n ],\n [\n -124.43115234375,\n 44.308126684886126\n ],\n [\n -124.60693359374999,\n 43.29320031385282\n ],\n [\n -124.78271484375,\n 42.4234565179383\n ],\n [\n -124.47509765625,\n 41.36031866306708\n ],\n [\n -124.5849609375,\n 40.245991504199026\n ],\n [\n -124.16748046874999,\n 39.90973623453719\n ],\n [\n -124.03564453125,\n 39.30029918615029\n ],\n [\n -123.53027343749999,\n 38.238180119798635\n ],\n [\n -123.20068359374999,\n 37.75334401310656\n ],\n [\n -122.78320312499999,\n 37.09023980307208\n ],\n [\n -122.1240234375,\n 36.73888412439431\n ],\n [\n -121.9921875,\n 35.871246850027966\n ],\n [\n -121.22314453124999,\n 35.38904996691167\n ],\n [\n -120.91552734375,\n 34.75966612466248\n ],\n [\n -120.62988281249999,\n 34.379712580462204\n ],\n [\n -120.34423828125,\n 34.32529192442733\n ],\n [\n -119.64111328125,\n 34.23451236236987\n ],\n [\n -119.091796875,\n 33.88865750124075\n ],\n [\n -118.47656249999999,\n 33.5963189611327\n ],\n [\n -117.83935546874999,\n 33.50475906922609\n ],\n [\n -112.027587890625,\n 34.43409789359469\n ],\n [\n -111.4892578125,\n 40.896905775860006\n ],\n [\n -115.8837890625,\n 43.866218006556394\n ],\n [\n -124.18945312500001,\n 44.731125592643274\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db61040a","contributors":{"authors":[{"text":"Kachadoorian, Reuben","contributorId":24336,"corporation":false,"usgs":true,"family":"Kachadoorian","given":"Reuben","email":"","affiliations":[],"preferred":false,"id":147578,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Yerkes, R. F.","contributorId":24754,"corporation":false,"usgs":true,"family":"Yerkes","given":"R.","middleInitial":"F.","affiliations":[],"preferred":false,"id":147579,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Waananen, Arvi O.","contributorId":34904,"corporation":false,"usgs":true,"family":"Waananen","given":"Arvi","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":147580,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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":68246,"text":"ha177 - 1967 - Availability of ground water in the Paducah West and East quadrangles, Illinois and Jackson Purchase region, Kentucky","interactions":[],"lastModifiedDate":"2021-10-06T19:39:10.177671","indexId":"ha177","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"177","title":"Availability of ground water in the Paducah West and East quadrangles, Illinois and Jackson Purchase region, Kentucky","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha177","usgsCitation":"Lambert, T.W., 1967, Availability of ground water in the Paducah West and East quadrangles, Illinois and Jackson Purchase region, Kentucky: U.S. Geological Survey Hydrologic Atlas 177, 2 Plates: 45.00 × 40.50 inches and 33.00 × 45.00 inches, https://doi.org/10.3133/ha177.","productDescription":"2 Plates: 45.00 × 40.50 inches and 33.00 × 45.00 inches","costCenters":[],"links":[{"id":189574,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":89627,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/177/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":89626,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/177/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":390290,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15539.htm"}],"scale":"24000","country":"United States","state":"Kentucky","otherGeospatial":"Paducah West and East quadrangles","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -88.75,37 ], [ -88.75,37.1275 ], [ -88.5,37.1275 ], [ -88.5,37 ], [ -88.75,37 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d8ea","contributors":{"authors":[{"text":"Lambert, T. William","contributorId":40574,"corporation":false,"usgs":true,"family":"Lambert","given":"T.","email":"","middleInitial":"William","affiliations":[],"preferred":false,"id":277903,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":63503,"text":"gp563 - 1967 - Aeromagnetic and inferred Precambrian paleogeologic map of east-central Minnesota and part of Wisconsin","interactions":[],"lastModifiedDate":"2022-04-11T19:25:03.65302","indexId":"gp563","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"563","title":"Aeromagnetic and inferred Precambrian paleogeologic map of east-central Minnesota and part of Wisconsin","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp563","usgsCitation":"Sims, P., and Zietz, I., 1967, Aeromagnetic and inferred Precambrian paleogeologic map of east-central Minnesota and part of Wisconsin: U.S. Geological Survey Geophysical Investigations Map 563, 1 Plate: 33.99 × 41.25 inches, https://doi.org/10.3133/gp563.","productDescription":"1 Plate: 33.99 × 41.25 inches","costCenters":[],"links":[{"id":398502,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_3519.htm"},{"id":179784,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0563/report-thumb.jpg"},{"id":100741,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0563/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":100740,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0563/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"250000","country":"United States","state":"Minnesota, Wisconsin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -94.6667,\n 44.5\n ],\n [\n -92.5,\n 44.5\n ],\n [\n -92.5,\n 46\n ],\n [\n -94.6667,\n 46\n ],\n [\n -94.6667,\n 44.5\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b02e4b07f02db69899c","contributors":{"authors":[{"text":"Sims, P.K.","contributorId":30191,"corporation":false,"usgs":true,"family":"Sims","given":"P.K.","email":"","affiliations":[],"preferred":false,"id":269001,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":269002,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":67979,"text":"ha266 - 1967 - Availability of water in eastern Saunders County, Nebraska","interactions":[],"lastModifiedDate":"2017-11-13T09:32:42","indexId":"ha266","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"266","title":"Availability of water in eastern Saunders County, Nebraska","docAbstract":"

The sand and gravel deposits of Quaternary age constitute the most important ground-water reservoir and are the source of nearly all the water pumped from wells in the area. An estimated 3.5 million acre-feet for good quality water is stored in these deposits and an additional 1.5 million acre-feet is stored in the underlying Dakota Sandstone. Even larger quantities are stored at greater depths in the Paleozoic dolomites and sandstones, but the water is of poorer quality. 

Pumpage for irrigation since 1956 is estimated to have ranged from about 2,500 acre-feet (1962) to about 6,000 acre-feet (1957). The town of Wahoo annually pumps about 460 acre-feet, and other towns pump an estimated total of 180 acre-feet. In 1963 the City of Lincoln pumped 27,000 acre-feet from its well field alongside the Platte River in the southeast corner of the area; since then pumpage has increased and probably is likely to continue to do so. Pumping at Lincoln city well field induces recharge from Platte River.

The quantity of ground water pumped to date is very small compared to the amount of water stored in the rocks. Furthermore, most of the ground water withdrawn has been replaced by infiltrating precipitation and by influent seepage from the Platte River. The large quantity of ground water in storage in addition to the flow of the Platte River indicates that the water resources of the area, if managed properly, can be developed much more extensively without appreciably depleting the supply.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha266","collaboration":"Prepared in cooperation with the Conservation and Survey Division of the University of Nebraska","usgsCitation":"Souders, V.L., 1967, Availability of water in eastern Saunders County, Nebraska: U.S. Geological Survey Hydrologic Atlas 266, Plate: 51.95 x 34.79 inches, https://doi.org/10.3133/ha266.","productDescription":"Plate: 51.95 x 34.79 inches","costCenters":[],"links":[{"id":89215,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/266/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":186138,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ha/266/report-thumb.jpg"}],"scale":"125000","country":"United States","state":"Nebraska","county":"Saunders County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.95297241210938,\n 41.01202954845378\n ],\n [\n -96.30889892578125,\n 41.01202954845378\n ],\n [\n -96.30889892578125,\n 41.447873389865194\n ],\n [\n -96.95297241210938,\n 41.447873389865194\n ],\n [\n -96.95297241210938,\n 41.01202954845378\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d5cc","contributors":{"authors":[{"text":"Souders, Vernon L.","contributorId":95145,"corporation":false,"usgs":true,"family":"Souders","given":"Vernon","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":277441,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":68194,"text":"ha237 - 1967 - Water resources of the Two Rivers Watershed, Northwestern Minnesota","interactions":[],"lastModifiedDate":"2018-03-19T10:03:34","indexId":"ha237","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"237","title":"Water resources of the Two Rivers Watershed, Northwestern Minnesota","docAbstract":"

The Two Rivers watershed includes two physiographic areas a lake plain and a till plain – within its 1,232 square miles.

\n

It lies in parts of Kittson and Roseau counties and includes the drainage basins of the Two Rivers and Joe River. The flat lake plain which extends 15 to 20 miles east of the Red River of the North is extensively cultivated for small grains and sugar beets. The gently undulating till plain is cultivated largely for small grains and hay. The areas not under cultivation support a forest of poplar with some maple and oak. Oak is the predominate tree on the sandy ridges. The large peat areas are covered with brush and marsh grasslands. Outdoor recreational facilities in the watershed consist principally of the Lake Bronson Park, water-fowl hunting in the extensive marshlands, and deer and small game hunting in the forested areas.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ha237","collaboration":"Prepared in cooperation with the Minnesota Department of Conservation, Division of Waters","usgsCitation":"Maclay, R., Winter, T.C., and Pike, G., 1967, Water resources of the Two Rivers Watershed, Northwestern Minnesota: U.S. Geological Survey Hydrologic Atlas 237, 8 Plates: 40 x 40 inches or smaller, https://doi.org/10.3133/ha237.","productDescription":"8 Plates: 40 x 40 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science 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C.","contributorId":84736,"corporation":false,"usgs":true,"family":"Winter","given":"Thomas","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":277821,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pike, G.M.","contributorId":80359,"corporation":false,"usgs":true,"family":"Pike","given":"G.M.","email":"","affiliations":[],"preferred":false,"id":277820,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":52573,"text":"ofr6771 - 1967 - Ground-water aspects of the lower Henrys Fork region, Idaho","interactions":[],"lastModifiedDate":"2013-11-19T10:29:25","indexId":"ofr6771","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":"67-71","title":"Ground-water aspects of the lower Henrys Fork region, Idaho","docAbstract":"The lower Henrys Fork region includes the plains and low benches between Ashton and the junction of Henrys Fork and Snake River in eastern Idaho. The northwestern and western parts of the area are part of the Snake River lava plain. The central part of the area is occupied by alluvial plains of the Snake, Teton, and Falls Rivers, and Henrys Fork. The southeastern part of the area is a bench (Rexburg Bench), chiefly on silicic and basaltic volcanic rocks, which rises gradually to mountain peaks southeast of the area. The basalt, and the sand and gravel under the alluvial plains are good aquifers and yield large amounts of water with small drawdowns. The silicic volcanic rocks and the interbedded ash, pyroclastics, and sedimentary deposits generally yield much less water than the basalt and alluvium. The regional water table slopes southward beneath the basalt and alluvial plains. Seepage from stream channels and irrigated tracts has resulted in an extensive body of ground water perched above the regional water table. The perched water in part moves vertically down to the regional water table and in part laterally to the streams. Ground water beneath the Rexburg Bench moves generally northwestward to join the regional ground-water body beneath the alluvial plain. The regional water table is below the level of the streams in the area and ground water in the main aquifer, therefore is not tributary to the streams. Recharge to the regional water table is estimated to average 725,000 acre-feet annually. Pumping from the regional ground-water reservoir for irrigation or other uses would have no effect on streamflow or surface-water rights within the study area. However, depletion of the underflow would eventually reduce the inflow to American Falls Reservoir unless the depletion was offset by additional recharge. Total withdrawals of ground water for irrigation in 1962 were estimated to be 25,000 acre-feet and caused no significant decline in the water table. In the Ashton area surface-water irrigation has cause water to be perched in basalt above the silicic volcanic rocks and much of this perched water contributed to streamflow. The flow of Henrys Fork would be decreased by the amount of pumped ground water consumed by crops. Ground-water prospects for irrigation in the Falls River area are not encouraging.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6771","collaboration":"Prepared in cooperation with the U.S. Bureau of Reclamation and Idaho Department of Reclamation","usgsCitation":"Crosthwaite, E., Mundorff, M., and Walker, E., 1967, Ground-water aspects of the lower Henrys Fork region, Idaho: U.S. Geological Survey Open-File Report 67-71, iii, 43 p., https://doi.org/10.3133/ofr6771.","productDescription":"iii, 43 p.","numberOfPages":"46","costCenters":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"links":[{"id":177408,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1967/0071/report-thumb.jpg"},{"id":86960,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0071/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","otherGeospatial":"Henry Fork Region","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -117.0,42.0 ], [ -117.0,49.0 ], [ -111.0,49.0 ], [ -111.0,42.0 ], [ -117.0,42.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d42a","contributors":{"authors":[{"text":"Crosthwaite, E.J.","contributorId":6525,"corporation":false,"usgs":true,"family":"Crosthwaite","given":"E.J.","email":"","affiliations":[],"preferred":false,"id":245569,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mundorff, M.J.","contributorId":48158,"corporation":false,"usgs":true,"family":"Mundorff","given":"M.J.","email":"","affiliations":[],"preferred":false,"id":245570,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Walker, E.H.","contributorId":104088,"corporation":false,"usgs":true,"family":"Walker","given":"E.H.","email":"","affiliations":[],"preferred":false,"id":245571,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":68429,"text":"ha246 - 1967 - Floods at Easton, Pennsylvania-Phillipsburg, New Jersey","interactions":[{"subject":{"id":52464,"text":"ofr6557 - 1965 - Extent and frequency of floods in the vicinity of Easton, Pennsylvania-Phillipsburg, New Jersey","indexId":"ofr6557","publicationYear":"1965","noYear":false,"title":"Extent and frequency of floods in the vicinity of Easton, Pennsylvania-Phillipsburg, New Jersey"},"predicate":"SUPERSEDED_BY","object":{"id":68429,"text":"ha246 - 1967 - Floods at Easton, Pennsylvania-Phillipsburg, New Jersey","indexId":"ha246","publicationYear":"1967","noYear":false,"title":"Floods at Easton, Pennsylvania-Phillipsburg, New Jersey"},"id":1}],"lastModifiedDate":"2023-03-07T22:04:51.913637","indexId":"ha246","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"246","title":"Floods at Easton, Pennsylvania-Phillipsburg, New Jersey","docAbstract":"

No abstract available.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha246","usgsCitation":"Farlekas, G.M., 1967, Floods at Easton, Pennsylvania-Phillipsburg, New Jersey: U.S. Geological Survey Hydrologic Atlas 246, 1 Plate: 39.50 x 37.00 inches, https://doi.org/10.3133/ha246.","productDescription":"1 Plate: 39.50 x 37.00 inches","costCenters":[],"links":[{"id":186616,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":413795,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15612.htm","linkFileType":{"id":5,"text":"html"}},{"id":89955,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/246/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"New Jersey, Pennsylvania","city":"Easton, Phillipsburg","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.25,\n 40.583\n ],\n [\n -75.25,\n 40.75\n ],\n [\n -75.125,\n 40.75\n ],\n [\n -75.125,\n 40.583\n ],\n [\n -75.25,\n 40.583\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e725d","contributors":{"authors":[{"text":"Farlekas, George M.","contributorId":44963,"corporation":false,"usgs":true,"family":"Farlekas","given":"George","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":278197,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221321,"text":"70221321 - 1967 - Stratigraphy and paleoenvironment of the phosphatic miocene strata of North Carolina","interactions":[],"lastModifiedDate":"2021-06-09T19:09:08.163317","indexId":"70221321","displayToPublicDate":"1967-12-01T14:04:13","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Stratigraphy and paleoenvironment of the phosphatic miocene strata of North Carolina","docAbstract":"

Foraminifera and Mollusca collected from the phosphatic Pungo River Formation and the overlying Yorktown Formation in eastern North Carolina were analyzed and interpreted for stratigraphic and environmental significance in order to determine optimum depositional sites for primary phosphorite. The Mollusca and benthonic foraminifera of the Pungo River Formation correlate with those of the Calvert Formation of Maryland, and the planktonic foraminifera in both of these formations correlate with the Globigerinatella insueta zone of Trinidad, postulated as late Aquitanian age. The paleoenvironment of the phosphorite deposition, interpreted primarily from the benthonic foraminifera, was of cool-temperate waters, ranging in depth from 100 to 200 m in the phosphatic beds to less than 70 m in the upper calcareous beds where phosphate is scarce. Phosphorite deposition occurred in an oceanic embayment located south of the Fort Monroe high in southern Virginia and north of a positive feature whose axis lies in the vicinity of New Bern, North Carolina. Cool-temperate waters in this area during Pungo River time indicate that circulation patterns of ocean currents and the resultant faunal provinces were not the same as those at present and later in the Miocene. In the Pungo River and its time equivalents of the Atlantic Coastal Plain, the presence of thick diatomaceous clay units, volcanic ash beds, shards, attapulgite clays, and other minerals probably derived from volcanic rocks, suggests a volcanic source somewhere off the coast during the Miocene. The Yorktown unconformably overlies the Pungo River Formation. The unconformity is marked by channels into the Pungo River, filled with phosphatic pebbles, vertebrate bones, and lower York-town molluscs and microfauna. The coarse-grained phosphatic material is derived from the underlying fine-grained primary phosphorite in the Pungo River and is abundant only in the lower part of the Yorktown Formation. Deposition of the lower part of the Yorktown occurred in waters about 100 m deep. The waters gradually became more shallow as deposition of the formation continued until depths of less than 15 m, and probable brackish conditions, were reached as the uppermost part of the formation was deposited. Temperature of the waters, cool-temperate during lower Yorktown deposition, became warm-temperate to subtropical in later Yorktown time. The faunal patterns suggest that circulation patterns reached their present state during late Yorktown time.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1967)78[631:SAPOTP]2.0.CO;2","usgsCitation":"Gibson, T., 1967, Stratigraphy and paleoenvironment of the phosphatic miocene strata of North Carolina: Geological Society of America Bulletin, v. 78, no. 5, p. 631-650, https://doi.org/10.1130/0016-7606(1967)78[631:SAPOTP]2.0.CO;2.","productDescription":"20 p.","startPage":"631","endPage":"650","costCenters":[],"links":[{"id":386367,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"North Carolina","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.8056640625,\n 36.61552763134925\n ],\n [\n -81.6943359375,\n 36.686041276581925\n ],\n [\n -83.78173828125,\n 35.55010533588552\n ],\n [\n -84.30908203125,\n 35.08395557927643\n ],\n [\n -84.30908203125,\n 34.97600151317588\n ],\n [\n -80.947265625,\n 35.137879119634185\n ],\n [\n -80.70556640625,\n 34.813803317113155\n ],\n [\n -79.6728515625,\n 34.77771580360469\n ],\n [\n -78.5302734375,\n 33.88865750124075\n ],\n [\n -78.0908203125,\n 33.925129700072\n ],\n [\n -76.201171875,\n 34.831841149828655\n ],\n [\n -75.52001953125,\n 35.764343479667176\n ],\n [\n -75.8056640625,\n 36.61552763134925\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"78","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Gibson, T. G.","contributorId":103702,"corporation":false,"usgs":true,"family":"Gibson","given":"T. G.","affiliations":[],"preferred":false,"id":817299,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221357,"text":"70221357 - 1967 - Stratigraphy and correlation of the precambrian belt supergroup of the southern Lewis and Clark Range, Montana","interactions":[],"lastModifiedDate":"2021-06-11T13:11:40.084744","indexId":"70221357","displayToPublicDate":"1967-12-01T08:01:34","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Stratigraphy and correlation of the precambrian belt supergroup of the southern Lewis and Clark Range, Montana","docAbstract":"

Several well-exposed and little-deformed Belt Supergroup sections have been studied in the southern Lewis and Clark Range. In the area studied, the Belt thins eastward or northeastward due both to primary sedimentation and to pre-Middle Cambrian erosion. These rocks can now be more precisely correlated with the well-known sections near Bonner, Helena, and Glacier National Park. In the western part of the area, the Missoula Group is thickest and lithologically intermediate between the sections at Bonner and Marias Pass. Formation names from these two sections are applied in the southern Lewis and Clark Range. The thin Belt sequence in the eastern part of the area includes the lower part of the Missoula Group and older formations that may be traced southward into the Helena, Empire, and Spokane Formations of the Helena area. Consequently, the Helena Dolomite of the Helena area, the Siyeh Formation of the Marias Pass area, and the \"Newland Limestone\" of the Bonner area are probably lateral equivalents.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1967)78[343:SACOTP]2.0.CO;2","usgsCitation":"McGill, G., and Sommers, D.A., 1967, Stratigraphy and correlation of the precambrian belt supergroup of the southern Lewis and Clark Range, Montana: Geological Society of America Bulletin, v. 78, no. 3, p. 343-352, https://doi.org/10.1130/0016-7606(1967)78[343:SACOTP]2.0.CO;2.","productDescription":"10","startPage":"343","endPage":"352","costCenters":[],"links":[{"id":386419,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","otherGeospatial":"Lewis and Clark range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.70898437499999,\n 46.24824991289166\n ],\n [\n -109.654541015625,\n 46.24824991289166\n ],\n [\n -109.654541015625,\n 47.331377157798244\n ],\n [\n -111.70898437499999,\n 47.331377157798244\n ],\n [\n -111.70898437499999,\n 46.24824991289166\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"78","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"McGill, G.E.","contributorId":14436,"corporation":false,"usgs":true,"family":"McGill","given":"G.E.","email":"","affiliations":[],"preferred":false,"id":817417,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sommers, David A.","contributorId":96761,"corporation":false,"usgs":true,"family":"Sommers","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":817418,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010485,"text":"70010485 - 1967 - Enclosed bark as a pollen trap","interactions":[],"lastModifiedDate":"2026-02-09T15:58:48.987708","indexId":"70010485","displayToPublicDate":"1967-09-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Enclosed bark as a pollen trap","docAbstract":"

Counts were made of pollen in traps formed by enclosed bark in two remnants of bristlecone pine, Pinus aristata Engelm., from the White Mountains of east-central California. The traps, dated by tree-rings at A.D. 350 and 1300 B.C., contained a major complex of pine-sagebrush pollen and traces of other species, representing the equivalent of the present vegetation.

","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.157.3792.1067","issn":"00368075","usgsCitation":"Adam, D., Ferguson, C., and Lamarch, V., 1967, Enclosed bark as a pollen trap: Science, v. 157, no. 3792, p. 1067-1068, https://doi.org/10.1126/science.157.3792.1067.","productDescription":"2 p.","startPage":"1067","endPage":"1068","costCenters":[],"links":[{"id":219240,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"White Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.47740391404712,\n 37.84573086539517\n ],\n [\n -118.47740391404712,\n 37.24138647578789\n ],\n [\n -118.04023510512017,\n 37.24138647578789\n ],\n [\n -118.04023510512017,\n 37.84573086539517\n ],\n [\n -118.47740391404712,\n 37.84573086539517\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"157","issue":"3792","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a091be4b0c8380cd51df2","contributors":{"authors":[{"text":"Adam, D.P.","contributorId":14815,"corporation":false,"usgs":true,"family":"Adam","given":"D.P.","email":"","affiliations":[],"preferred":false,"id":359031,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ferguson, C.W.","contributorId":37888,"corporation":false,"usgs":true,"family":"Ferguson","given":"C.W.","email":"","affiliations":[],"preferred":false,"id":359032,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lamarch, V.C. Jr.","contributorId":42348,"corporation":false,"usgs":true,"family":"Lamarch","given":"V.C.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":359033,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70209344,"text":"70209344 - 1967 - Post-paleozoic radiometric ages and their relevance to fault movements, Northern Southeastern Alaska","interactions":[],"lastModifiedDate":"2020-04-01T12:13:03","indexId":"70209344","displayToPublicDate":"1967-04-01T12:02:43","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Post-paleozoic radiometric ages and their relevance to fault movements, Northern Southeastern Alaska","docAbstract":"

Recently determined lead-alpha and potassium-argon ages from northern southeastern Alaska indicate major plutonic events in the Paleozoic, Mesozoic, and Tertiary; in contrast, previous studies suggested that only one complex Jurassic and Cretaceous event occurred. The ages presented in this paper indicate the following Mesozoic and Tertiary plutonic events: Middle or Late Jurassic (144–164 m.y.); Early Cretaceous (103–117 m.y.); Eocene (42–48 m.y.); and Oligocene to Miocene (24–31 m.y.). The present data show no distinctive a real pattern for the Mesozoic plutons, but those of known Tertiary age are restricted to Baranof and Kruzof islands, a distribution that suggests a belt of Tertiary plutonism along the margin of the Pacific Ocean.

Stratigraphic evidence and radiometric ages indicate that Baranof Island and possibly Chichagof Island have been uplifted several kilometers since Miocene time, whereas Admiralty Island to the east appears to have been relatively stable since Paleocene time. This movement apparently took place on the north-striking Chatham Strait fault, which separates the islands, and probably also had a large right-lateral component. Northwest-striking faults in Chichagof and Baranof islands were probably active during at least part of the movement on the Chatham Strait fault. Movement on one of the northwest-striking faults, the Patterson Bay fault of Baranof Island, took place some time between the Eocene and the Miocene and produced a 5-km, right-lateral separation.

The inferred uplift of Baranof Island relative to Admiralty Island is based on the present-day exposure on Baranof Island of mesozonal Tertiary plutons, which were probably intruded at a depth of several kilometers, contrasted with the present-day exposure on Admiralty Island of continental sedimentary and volcanic rocks that were being deposited near sea level during the Tertiary. The uplift of the Baranof Island plutons to the surface in post-Miocene time contrasts sharply with the stable or weakly negative tectonic conditions that have prevailed on Admiralty Island since the Paleocene.

","language":"English","publisher":"GSA","doi":"10.1130/0016-7606(1967)78[511:PRAATR]2.0.CO;2","usgsCitation":"Loney, R.A., Brew, D.A., and Lanphere, M.A., 1967, Post-paleozoic radiometric ages and their relevance to fault movements, Northern Southeastern Alaska: GSA Bulletin, v. 78, no. 4, p. 511-526, https://doi.org/10.1130/0016-7606(1967)78[511:PRAATR]2.0.CO;2.","productDescription":"16 p.","startPage":"511","endPage":"526","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":373712,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Northern Southeastern Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -136.7138671875,\n 54.09806018306312\n ],\n [\n -131.94580078125,\n 54.09806018306312\n ],\n [\n -131.94580078125,\n 58.297944045474146\n ],\n [\n -136.7138671875,\n 58.297944045474146\n ],\n [\n -136.7138671875,\n 54.09806018306312\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"78","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Loney, R. A.","contributorId":90757,"corporation":false,"usgs":true,"family":"Loney","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":786217,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brew, David A. dbrew@usgs.gov","contributorId":3244,"corporation":false,"usgs":true,"family":"Brew","given":"David","email":"dbrew@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":786218,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lanphere, Marvin A. alder@usgs.gov","contributorId":2696,"corporation":false,"usgs":true,"family":"Lanphere","given":"Marvin","email":"alder@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":786219,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70210851,"text":"70210851 - 1967 - Belt of sigmoidal bending and right-lateral faulting in the western great basin","interactions":[],"lastModifiedDate":"2020-06-29T16:56:25.742494","indexId":"70210851","displayToPublicDate":"1967-02-01T11:53:34","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Belt of sigmoidal bending and right-lateral faulting in the western great basin","docAbstract":"

Betweeen the northwest-trending Sierra Nevada and the north-northeast-trending ranges that characterize most of the Great Basin section of the Basin and Range province is a belt of confused and divergent topographic forms, which is approximately 50 miles wide and 300 miles long. Along the eastern part of this belt is a topographically low lineament called the Walker Lane.

A number of the ranges along the belt have an arcuate form which is controlled by the structure of rocks that are mainly of pre-Cretaceous age; locally, in the southern part of the belt, rocks as young as early Miocene show the arcuate form. The strike of tilted beds, fold axes, and in places elongate plutons, parallels the trend of the arcuate ranges, herein called “oroflexes”—defined as mountain ranges with arcuate trends that result from tectonic bending of the crust.

The gross structural pattern of pre-middle Miocene rocks along the belt is a series of sigmoidal bends that suggest gigantic dextral drag. The sigmoidal bends define the oroflexes, facies boundaries, and structural trend lines. These features are cut in places by at least three, and probably five, major northwest-trending faults having right-lateral separations of many miles. Along the strike, the two largest faults seem to die out and the movement is believed to be taken up by bending.

The indicated total horizontal displacement by bending and faulting along the belt is 80–120 miles, the Great Basin having moved southeastward relative to the Sierra Nevada. This movement is most likely restricted to the crust, which at some depth is thought to have moved freely over deeper material —either a deeper segment of the crust or the mantle.

Available evidence permits the interpretation that the deformation began possibly as early as late Early Jurassic and that the same movement pattern has prevailed ever since. The bending and major strike-slip faulting must have been completed by early or middle Miocene time but much of it may have taken place as long ago as the Jurassic. More recent movements have been restricted to faulting.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1967)78[143:BOSBAR]2.0.CO;2","usgsCitation":"Albers, J., 1967, Belt of sigmoidal bending and right-lateral faulting in the western great basin: GSA Bulletin, v. 78, no. 2, p. 143-156, https://doi.org/10.1130/0016-7606(1967)78[143:BOSBAR]2.0.CO;2.","productDescription":"14 p.","startPage":"143","endPage":"156","costCenters":[],"links":[{"id":375986,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Great Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.06005859375,\n 41.96765920367816\n ],\n [\n -120.05859375,\n 42.01665183556825\n ],\n [\n -120.05859375,\n 39.095962936305476\n ],\n [\n -118.16894531249999,\n 37.64903402157866\n ],\n [\n -117.8173828125,\n 35.06597313798418\n ],\n [\n -114.60937499999999,\n 34.939985151560435\n ],\n [\n -114.71923828124999,\n 36.08462129606931\n ],\n [\n -114.12597656249999,\n 36.10237644873644\n ],\n [\n -114.06005859375,\n 41.96765920367816\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"78","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Albers, John P.","contributorId":55291,"corporation":false,"usgs":true,"family":"Albers","given":"John P.","affiliations":[],"preferred":false,"id":791707,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16484,"text":"ofr879_1967 - 1967 - Mineral appraisal of the Flattery Rocks, Quillayute Needles, and Copalis National Wildlife Refuges, Washington","interactions":[],"lastModifiedDate":"2024-09-17T17:42:29.300705","indexId":"ofr879_1967","displayToPublicDate":"1967-01-01T16:05:24","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":"879","title":"Mineral appraisal of the Flattery Rocks, Quillayute Needles, and Copalis National Wildlife Refuges, Washington","docAbstract":"

The Flattery Rocks, Quillayute Needles, and Copalis National Wildlife Refuges lie off the Pacific coast of the Olympic Peninsula between Cape Flattery and Grays Harbor. They have a total land area of 247 acres and consists of numerous small islands, sea stacks and rocks that rise above a wave-cut platform. The refuges are in a belt of intensely folded and faulted marine sedimentary and volcanic rocks of early Eocene to Pliocene age. Pleistocene glaciofluvial deposits blanket the Tertiary strata along this coastal belt. The disturbed belt borders the eastern margin of a depositional basin on the continental shelf that probably contains a thick sequence of late Tertiary rocks.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr879_1967","usgsCitation":"Weissenborn, A.E., and Snavely, P.D., 1967, Mineral appraisal of the Flattery Rocks, Quillayute Needles, and Copalis National Wildlife Refuges, Washington: U.S. Geological Survey Open-File Report 879, 30 p., https://doi.org/10.3133/ofr879_1967.","productDescription":"30 p.","costCenters":[],"links":[{"id":417115,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/879_1967/report-thumb.jpg"},{"id":417330,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8872.htm","linkFileType":{"id":5,"text":"html"}},{"id":434871,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/879_1967/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Washington","otherGeospatial":"Copalis National Wildlife Refuge, Flattery Rocks National Wildlife Refuge, Quillayute Needles National Wildlife Refuge","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -124.77391836685513,\n 48.1815019611561\n ],\n [\n -124.77391836685513,\n 48.15030925780698\n ],\n [\n -124.73338665471016,\n 48.15030925780698\n ],\n [\n -124.73338665471016,\n 48.1815019611561\n ],\n [\n -124.77391836685513,\n 48.1815019611561\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -124.46562950263186,\n 47.83854729846999\n ],\n [\n -124.5104214830809,\n 47.83854729846999\n ],\n [\n -124.5104214830809,\n 47.82039144984293\n ],\n [\n -124.46562950263186,\n 47.82039144984293\n ],\n [\n -124.46562950263186,\n 47.83854729846999\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -124.3384552486784,\n 47.44579550453264\n ],\n [\n -124.35453823958551,\n 47.44579550453264\n ],\n [\n -124.35453823958551,\n 47.42648577612718\n ],\n [\n -124.3384552486784,\n 47.42648577612718\n ],\n [\n -124.3384552486784,\n 47.44579550453264\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Weissenborn, Albert Edward","contributorId":98698,"corporation":false,"usgs":true,"family":"Weissenborn","given":"Albert","email":"","middleInitial":"Edward","affiliations":[],"preferred":false,"id":510897,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Snavely, Parke Detweiler Jr.","contributorId":48535,"corporation":false,"usgs":true,"family":"Snavely","given":"Parke","suffix":"Jr.","email":"","middleInitial":"Detweiler","affiliations":[],"preferred":false,"id":872863,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70114650,"text":"70114650 - 1967 - Results of the second phase of the drought-disaster test-drilling program near Morristown, N.J.","interactions":[],"lastModifiedDate":"2018-01-08T18:31:02","indexId":"70114650","displayToPublicDate":"1967-01-01T13:17:37","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":149,"text":"New Jersey Division of Water Policy and Supply Water Resources Circular","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"17","title":"Results of the second phase of the drought-disaster test-drilling program near Morristown, N.J.","docAbstract":"

The continued drought in northeastern New Jersey through the summer of 1966 with its attendant water-supply problems resulted in an extension of the drought-disaster test-drilling program originally requested by the Office of Emergency Planning on August 30, 1965. Authorization to continue test drilling was fiven by the Office of Emergency Planning on September 26, 1966, with the stipulation that all field work be complete by January 31, 1977. Contractural costs were paid by the Office of Emergency Planning, whereas personnel costs were shared by the U.S. Geological Survey and the New Jersey Department of Conservation and Economic Development, Division of Water Policy and Supply.

The work undertaken in 1965 by the Geological Survey was \"...to preform the necessary drilling and testing of wells to identify the extent and nature of a reserve ground-water source in the vicinity of the Passaic River near the northern New Jersey metropolitan area.\" Results of this first phase were made available in the fall of 1966 in Water Resources Circular 16 of the New Jersey Department of Conservation and Economic Development. Three of the five areas tested (figure 1)--two in Parsippany-Troy Hills Township (areas 2 and 4) and one in East Hanover Township (area 1), Morris County--proved capable of providing an aggregate sustained yield of 7.5 million gallons daily (mgd) from wells constructed in sand and gravel deposits. Because significant supplies of ground water for emergency use were located in the first phase of the exploratory test-drilling program, it was though desirable to extend the originally planned studies so as to obtain maximum practicable information on emergency supplies.

During this second phase of the investigation, drilling was conducted in 16 sites in Chatham, Madison, and Florham Park Boroughs and in Hanover and East Hanover Townships, Morris County. (See figure 2.) The drilling in Hanover and East Hanover Townships, and part of the drilling done in Florham Park was to explore the availability of large undeveloped ground-water supplies. Drilling in Chatham, Madison, and Florham Park Boroughs was done primarily to determine the extent and continuity of buried valley-fill aquifers, so that a full evaluation of the effects of pumpage from other areas on these already heavily pumped areas could be made. In addition, it was anticipated that the drilling could help in defining the feasibility of artificial recharge of the heavily pumped areas and in the determination of the prospective method of recharge and points of emplacement.

Arrangements for easements with landowners, preparation of specifications for well drilling and seismic work, and supervision of well drilling and seismic contracts were all performed by the New Jersey District, Water Resources Division of the Geological Survey.

Prior to the test drilling, seismic exploration under contract with Alpine Geophysical Associates of Norwood, N. J. was conducted at five locations in the Chatham-Madison-Florham Park area and at one place in Parsippany-Troy Hills Township. The seismic work was done to determine the most favorable location for a test well at several potential test-well sites and to help in the interpretation of subsurface geology between test sites.

Contracts for the drilling of the test holes were awarded during November and drilling commences on November 30. Kaye Well drilling, Inc. of Jackson, N. J. was the recipient of a contract for eight of the test holes, and a second contract was awarded to Rinbrand Well Drilling Co., Inc. of Glen Rock, N. J.--also for eight test holes.

Acknowledgment is due to the many public officials of Chatham, Madison, Florham Park, Morristown, and East Hanover Township as well as officials of the Braidburn Corporation and Esso Research and Engineering Co., who cooperated by making their lands available for exploration.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Trenton, NJ","collaboration":"Prepared by the State of New Jersey Department of Conservation and Economic Development, Division of Water Policy and Supply, in cooperation with United States Department of the Interior Geological Survey","usgsCitation":"Vecchioli, J., Nichols, W., and Nemickas, B., 1967, Results of the second phase of the drought-disaster test-drilling program near Morristown, N.J.: New Jersey Division of Water Policy and Supply Water Resources Circular 17, Report: v, 23 p.; 3 Plates: 34.65 x 21.48 inches or smaller.","productDescription":"Report: v, 23 p.; 3 Plates: 34.65 x 21.48 inches or smaller","numberOfPages":"30","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":290164,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":327417,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70114650/figure-4.pdf","text":"Figure 4","linkFileType":{"id":1,"text":"pdf"}},{"id":327415,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70114650/figure-2.pdf","text":"Figure 2","linkFileType":{"id":1,"text":"pdf"}},{"id":327416,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70114650/figure-3.pdf","text":"Figure 3","linkFileType":{"id":1,"text":"pdf"}},{"id":290163,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70114650/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Jersey","city":"Morristown","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -74.501444,40.780231 ], [ -74.501444,40.818361 ], [ -74.456181,40.818361 ], [ -74.456181,40.780231 ], [ -74.501444,40.780231 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ad40f9e4b0729c154181d6","contributors":{"authors":[{"text":"Vecchioli, John","contributorId":36113,"corporation":false,"usgs":true,"family":"Vecchioli","given":"John","email":"","affiliations":[],"preferred":false,"id":495394,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nichols, William D.","contributorId":98296,"corporation":false,"usgs":true,"family":"Nichols","given":"William D.","affiliations":[],"preferred":false,"id":495395,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nemickas, Bronius","contributorId":105733,"corporation":false,"usgs":true,"family":"Nemickas","given":"Bronius","email":"","affiliations":[],"preferred":false,"id":495396,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70039249,"text":"70039249 - 1967 - Mountains and plains Denver's geologic setting","interactions":[],"lastModifiedDate":"2012-08-03T01:02:04","indexId":"70039249","displayToPublicDate":"1967-01-01T13:01:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":362,"text":"General Information Product","active":false,"publicationSubtype":{"id":6}},"title":"Mountains and plains Denver's geologic setting","docAbstract":"A slice of geologic history is exposed to view in the Denver, Colorado area. Denver is situated on the High Plains near the east front of the Rocky Mountains. As one travels westward from Denver toward the mountains, successively older rocks are crossed from the geologically young rocks of the High Plains and the South Platte River valley to the older rocks of the foothills and the ancient rocks of the mountains. Thus, within a few miles,the journey turns back the pages of time in a lifesized textbook that vividly illustrates the geologic events that shaped the landscape.","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/70039249","usgsCitation":"Water Resources Division, U.S. Geological Survey, 1967, Mountains and plains Denver's geologic setting: General Information Product, 23 p., https://doi.org/10.3133/70039249.","productDescription":"23 p.","numberOfPages":"24","costCenters":[],"links":[{"id":261472,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gip/70039249/report.pdf"},{"id":261473,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gip/70039249/report-thumb.jpg"}],"country":"United States","state":"Colorado","city":"Denver","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -106.25,38.833333333333336 ], [ -106.25,40.583333333333336 ], [ -103.5,40.583333333333336 ], [ -103.5,38.833333333333336 ], [ -106.25,38.833333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5ebae4b0c8380cd70c33","contributors":{"authors":[{"text":"Water Resources Division, U.S. Geological Survey","contributorId":128075,"corporation":true,"usgs":false,"organization":"Water Resources Division, U.S. Geological Survey","id":535271,"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":"

This study of the geometry of limestone solution is based on the following conditions: (1) the limestone is impermeable but contains and transmits water in joints, fractures, bedding‐plane partings, and solution channels; (2) at depth, the limestone aquifer is underlain by impermeable rock; (3) ground water in the limestone is under water‐table conditions; (4) recharge to the limestone 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 limestone through which it flows, continuously modifying the flow pattern and the hydrologic properties of the medium. These conditions commonly are found in limestone terranes in the eastern and central United States. An electrical analog 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 limestone solution and changes in ground‐water flow in the aquifer. The initial analog 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 analog study support the following conclusions: (1) The most active zone of solution 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, solution channels have a greater lateral than vertical extent.

","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":70201217,"text":"70201217 - 1967 - Mineral appraisal of the Poker Jim Ridge and Fort Warner areas of the Hart Mountain National Antelope Refuge, Lake County, Oregon","interactions":[],"lastModifiedDate":"2018-12-11T10:22:12","indexId":"70201217","displayToPublicDate":"1967-01-01T11:21:39","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":"Mineral appraisal of the Poker Jim Ridge and Fort Warner areas of the Hart Mountain National Antelope Refuge, Lake County, Oregon","docAbstract":"

The Poker Jim Ridge and Fort Warner areas, which are candidate areas for inclusion in the National Wilderness Preservation System, are in the Hart Mountain National Antelope Refuge in east-central Lake County, south-central Oregon. The two areas form part of an upraised and tilted fault block--a structural element that is typical of the northern part of the Great Basin province. Rocks in the two areas are principally volcanic in origin. They have been faulted, uplifted, and tilted eastward, the older rocks having been more strongly deformed than the younger ones.

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/70201217","usgsCitation":"Walker, G.W., and Swanson, D., 1967, Mineral appraisal of the Poker Jim Ridge and Fort Warner areas of the Hart Mountain National Antelope Refuge, Lake County, Oregon: Open-File Report, iii, 28 p., https://doi.org/10.3133/70201217.","productDescription":"iii, 28 p.","costCenters":[],"links":[{"id":360142,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70201217/report-thumb.jpg"},{"id":360143,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70201217/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Oregon","county":"Lake County","otherGeospatial":"Hart Mountain National Antelope Refuge","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.81964111328124,\n 42.33418438593939\n ],\n [\n -119.34173583984375,\n 42.33418438593939\n ],\n [\n -119.34173583984375,\n 42.742978093466434\n ],\n [\n -119.81964111328124,\n 42.742978093466434\n ],\n [\n -119.81964111328124,\n 42.33418438593939\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5c10dadfe4b034bf6a7fcc63","contributors":{"authors":[{"text":"Walker, George W.","contributorId":101308,"corporation":false,"usgs":true,"family":"Walker","given":"George","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":753762,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Swanson, Donald A. 0000-0002-1680-3591 donswan@usgs.gov","orcid":"https://orcid.org/0000-0002-1680-3591","contributorId":3137,"corporation":false,"usgs":true,"family":"Swanson","given":"Donald A.","email":"donswan@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":false,"id":753763,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70252069,"text":"70252069 - 1967 - Pre-Olympia Pleistocene stratigraphy and chronology in the central Puget Lowland, Washington","interactions":[],"lastModifiedDate":"2024-03-12T16:07:12.955763","indexId":"70252069","displayToPublicDate":"1967-01-01T10:50:36","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Pre-Olympia Pleistocene stratigraphy and chronology in the central Puget Lowland, Washington","docAbstract":"

Drifts of two pre-Olympia glaciations separated by nonglacial sediments are widespread in the central Puget Lowland of western Washington. The Double Bluff Drift (older) and Possession Drift represent advances of the Puget lobe of the Cordilleran ice sheet more than 40,000 years ago. The nonglacial Whidbey Formation between the drifts was formed in streams and lakes. During its deposition, climate was initially cool and moist, as inferred from pollen in peat beds, but subsequently it became much like that of the present in the lowland. The Possession Drift is tentatively correlated with glacial deposits of Salmon Springs age in the southern part of the lowland. The Whidbey Formation may correlate with nonglacial deposits between two Salmon Springs Drifts or with the Puyallup Formation.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1967)78[13:PPSACI]2.0.CO;2","usgsCitation":"Easterbrook, D.J., Crandell, D., and Leopold, E.B., 1967, Pre-Olympia Pleistocene stratigraphy and chronology in the central Puget Lowland, Washington: GSA Bulletin, v. 78, no. 1, p. 13-20, https://doi.org/10.1130/0016-7606(1967)78[13:PPSACI]2.0.CO;2.","productDescription":"8 p.","startPage":"13","endPage":"20","costCenters":[],"links":[{"id":426558,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","otherGeospatial":"Central Puget Lowland","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -122.13981196181514,\n 48.3375501570402\n ],\n [\n -122.85544279427498,\n 48.35045469190817\n ],\n [\n -122.85544279427498,\n 47.76461892070904\n ],\n [\n -122.13981196181516,\n 47.75902516658033\n ],\n [\n -122.13981196181514,\n 48.3375501570402\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"78","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Easterbrook, D. J.","contributorId":55089,"corporation":false,"usgs":true,"family":"Easterbrook","given":"D.","middleInitial":"J.","affiliations":[],"preferred":false,"id":896491,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crandell, Dwight R.","contributorId":75946,"corporation":false,"usgs":true,"family":"Crandell","given":"Dwight R.","affiliations":[],"preferred":false,"id":896492,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Leopold, Estella B.","contributorId":30979,"corporation":false,"usgs":true,"family":"Leopold","given":"Estella","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":896493,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70156254,"text":"70156254 - 1967 - Devonian of the Northern Rocky Mountains and plains","interactions":[],"lastModifiedDate":"2015-08-17T12:47:04","indexId":"70156254","displayToPublicDate":"1967-01-01T01:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Devonian of the Northern Rocky Mountains and plains","docAbstract":"

The Devonian System, represented predominantly by shallow-water marine carbonate, is widespread in Montana, Wyoming, eastern Idaho, North Dakota, South Dakota, and northwestern Nebraska. It comprises cratonic rocks in the east and miogeosynclinal rocks in the west.

\n

The cratonic rocks thicken generally northward from their southern limit in Wyoming across a broad shelf that occupies most of Wyoming and Montana. In northern Montana, they are as much as 1,250 feet thick. Cratonic rocks also thicken eastward from areas of Early Mississippian erosional thinning in central and eastern Montana to as much as 2,000 feet in the intracratonic Williston basin centered in northwestern North Dakota.

\n

The miogeosynclinal rocks, which moved eastward on low-angle thrust faults, abut against cratonic rocks along a north-trending disturbed belt in western Wyoming, western Montana and eastern Idaho. The miogeosynclinal rocks thicken abruptly westward from 1,000 feet near this belt to about 3,000 feet near the east edge of the Idaho batholith. Farther west they have been buried beneath younger rocks, altered by the batholith, or eroded.

\n

Five subdivisions of the Devonian System are treated separately:

\n

1. Upper Lower Devonian (Coblenzian) marginal and nearshore marine carbonate rocks and related continental and estuarine discontinuous sinkhole and channel-fill deposits.

\n

2. Upper Middle Devonian (Givetian) carbonate rocks that contain a 525-foot-thick evaporitic sequence in the Williston basin.

\n

3. Lower Upper Devonian (Frasnian, toI) cyclically deposited carbonate rocks that include thick beds of dolarenite and dolomitized calcarenite on the west.

\n

4. Upper Upper Devonian (Famennian, toII-IV) evaporitic rocks overlain by fossilferous open-marine shale and limestone.

\n

5. Undivided uppermost Devonian (Famennian, to V-VI) and lowermost Mississippian (Tournaisian, cuI-lower cuIIα) carbonaceous and clastic rocks deposited in six shallow basins interspersed among areas uplifted during the penecontemporaneous Antler orogeny.

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The structural framework that controlled Devonian deposition consisted of, from west to east: (1) a eugeosynclinal area in northern California and western Nevada; (2) a miogeosynclinal area in southeastern California, eastern Nevada, and western Utah; and (3) a cratonic area in Arizona, eastern Utah, Colorado, New Mexico, and western Texas, east of a northeast-trending hinge line (Wasatch line).

\n

The eugeosyncline contains a fragmentary record of Middle Devonian rocks at least 4,000 feet thick characterized by thin-bedded chert, siliceous mudstone, and some limestone and volcanic rocks. The original thickness, however, probably exceeded 6,000 feet and probably included Lower and Upper Devonian rocks. The miogeosyncline contains Lower, Middle, and Upper Devonian rocks as much as 6,000 feet thick characterized by thick units of dolomite and limestone and some local interbeds of sandstone. A transitional zone perhaps 50 miles wide separates the eugeosynclinal and miogeosynclinal facies. The craton contains mostly Upper Devonian rocks, generally less than 1,000 feet thick, characterized by dolomite and limestone and local interbeds of sandstone and mudstone.

\n

Widespread crustal movements occurred during Late Devonian time. The Antler orogeny in Nevada initiated a culm facies in the geosyncline. Eugeosynclinal and transitional rocks including those of Devonian age were uplifted to form the Antler orogenic belt, and then were thrust eastward over autochthonous miogeosynclinal rocks in latest Devonian or earliest Mississippian time. Folding and faulting, and subsequent erosion on local uplifts, produced clastic deposits of Late Devonian age in Utah and southwestern Colorado.

\n

Devonian rocks in many parts of the geosynclinal area have been moved since Devonian time by large-scale, generally eastward thrusting, oroflexural bending and strike-slip faulting.

\n

Four major subdivisions of the Devonian System and related rocks are treated separately:

\n

1) Lower Devonian (Gedinnian, Siegenian, Emsian) and related Upper Silurian (Ludlovian) rocks.

\n

2) Middle Devonian (Eifelian and Givetian) rocks.

\n

3) Lower Upper Devonian (Frasnian, to I) rocks.

\n

4) Upper Upper Devonian (Famennian, to II-VI) and related lowermost Mississippian (Tournaisian, cu I) rocks.

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