Gravity and seismic measurements in southern Owens Valley, California, have outlined a deep subsurface trough, bounded throughout the greater part of its length by steep faults. Depths to the bedrock floor along the central part of the valley range from 3,000 to 9,000 ft below the surface. The subsurface trough is divided into two parts, a narrow channel-like depression near Lone Pine bounded by northwest-trending faults, and a broad basin at Owens Lake bounded by a more complex series of border faults. The bedrock ridge that crops out to form Alabama Hills is shown to extend from Independence to the north edge of Owens Lake, nearly twice its visible extent. The main direction of faults that have formed the valley is northwest; subsidiary faults trend north, northeast, and east. A fairly sharp velocity boundary within the Cenozoic valley deposits suggests a change in the rate and character of deposition which was probably the result of renewed uplift in the nearby mountains.
","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1438835","usgsCitation":"Kane, M.F., and Pakisek, L., 1961, Geophysical study of subsurface structure in southern Owens Valley, California: Geophysics, v. 26, no. 1, p. 12-26, https://doi.org/10.1190/1.1438835.","productDescription":"15 p.","startPage":"12","endPage":"26","costCenters":[],"links":[{"id":385825,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Owens Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -120.33325195312499,\n 37.74465712069939\n ],\n [\n -119.46533203125,\n 37.74465712069939\n ],\n [\n -119.46533203125,\n 39.45316112807394\n ],\n [\n -120.33325195312499,\n 39.45316112807394\n ],\n [\n -120.33325195312499,\n 37.74465712069939\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"26","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Kane, M. F.","contributorId":45708,"corporation":false,"usgs":true,"family":"Kane","given":"M.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":816143,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pakisek, L.C.","contributorId":258180,"corporation":false,"usgs":false,"family":"Pakisek","given":"L.C.","email":"","affiliations":[],"preferred":false,"id":816144,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220645,"text":"70220645 - 1961 - Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming","interactions":[],"lastModifiedDate":"2021-05-21T19:21:30.166576","indexId":"70220645","displayToPublicDate":"1961-12-31T14:17:30","publicationYear":"1961","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":"Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming","docAbstract":"Normal faults offset a bedrock surface scoured by Pleistocene ice in several areas within and south of Yellowstone National Park. Recurrent earthquake shocks and fresh appearance of some scarps suggest that movement is continuing along some faults. Four systems of faults are described. Quaternary movement occurred along more than 60 faults on the Mirror Plateau, 15 miles northeast of Yellowstone Lake. Faults trend northwest, and several are more than 6 miles long. Maximum displacement exceeds 250 feet. The majority have northeast blocks downdropped, but some grabens and horsts are present. Eocene to Pliocene igneous or pyroclastic rocks are displaced. Ice moved southwest and south from the Beartooth and Absaroka ranges, nearly at right angles to the fault trends. Drainage in many ice-scoured valleys was disrupted by faulting, and small lakes (such as Mirror Lake) formed on downthrown blocks. Thermal activity occurs along some of these faults. Directly east of Mirror Plateau, the Lamar normal fault has a displacement of 1300 + feet; perhaps 1000 feet of this may have occurred during Quaternary time. The Yellowstone Falls fault system cuts Pliocene rhyolite southeast of the Upper Falls of the Yellowstone River. Faults trend northwest; maximum displacement exceeds 200 feet. The Solfatara fault system trends north-northwest, cuts Pliocene rhyolite, and has a maximum Quaternary displacement of about 200 feet. The Hering Lake fault system is a northern extension of the Teton fault, trends northward, and cuts Pliocene rhyolite and rhyolitic welded tuff. Maximum displacement is about 200 feet. West-flowing streams established on bedrock scoured by ice were disrupted, and Beula, Hering, and South Boundary lakes formed on the downthrown (east) blocks. The sharp angular unstepped appearance of fault scarps 50 to 200 feet high in these fault systems suggests that each scarp of this type was formed by one continuous movement. The displacement along faults associated with the Hebgen earthquake of August 1959 is commonly less than 20 feet. The abundance of Quaternary faults and the record of 18 earthquakes in historic time suggest that additional faulting and earthquake activity can be expected in the future. Recognition of this probability should influence the location and type of construction of buildings and other facilities.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1749:RSOQFI]2.0.CO;2","usgsCitation":"Love, D., 1961, Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming: Geological Society of America Bulletin, v. 72, no. 12, p. 1749-1764, https://doi.org/10.1130/0016-7606(1961)72[1749:RSOQFI]2.0.CO;2.","productDescription":"16 p.","startPage":"1749","endPage":"1764","costCenters":[],"links":[{"id":480377,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://figshare.com/articles/figure/Reconnaissance_study_of_Quaternary_faults_in_and_south_of_Yellowstone_National_Park_Wyoming/13687621","text":"External Repository"},{"id":385865,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"Yellowstone National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.03881835937499,\n 43.6599240747891\n ],\n [\n -108.797607421875,\n 43.6599240747891\n ],\n [\n -108.797607421875,\n 45.01141864227728\n ],\n [\n -111.03881835937499,\n 45.01141864227728\n ],\n [\n -111.03881835937499,\n 43.6599240747891\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Love, D.","contributorId":15809,"corporation":false,"usgs":true,"family":"Love","given":"D.","email":"","affiliations":[],"preferred":false,"id":816284,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220644,"text":"70220644 - 1961 - Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana","interactions":[],"lastModifiedDate":"2021-05-21T19:16:21.510182","indexId":"70220644","displayToPublicDate":"1961-12-31T14:08:45","publicationYear":"1961","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":"Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana","docAbstract":"Douglass Creek basin lies west of the Continental Divide in the northern part of the Rocky Mountain physiographic province. Numerous minor environmental differences exist between the Douglass Creek area and the Pipestone Springs and Canyon Ferry areas east of the Divide. In the 19th century, however, the three areas had identical mammalian species representation, although not equally dense populations. Fossils of an early Oligocene biota have been collected from the Douglass Creek basin. Presence of all but one of the Douglass Creek mammalian species in the Pipestone Springs-Canyon Ferry early Oligocene fauna suggests that the three ancient ecosystems resembled each other in much the same way as the 19th century systems. The early Oligocene deposits and biota of the Douglass Creek basin indicate a moist, temperate climate with seasonal variations. Sediment size and distribution suggest that the cross-valley relief was no greater than it is now. The fish and invertebrate faunas show that a shallow, hard-water lake existed in the area. The flora included a lowland, lake-border association and an upland coniferous forest. Although the ancient Douglass Creek biota doubtless included many species not represented in the fossil collections, most of the mammalian species are probably represented in the combined Douglass Creek, Pipestone Springs, and Canyon Ferry fossil assemblages. If so, the number of mammalian species was about the same as in the 19th century ecosystem.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1633:POAEOB]2.0.CO;2","usgsCitation":"Konizeski, R.L., 1961, Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana: Geological Society of America Bulletin, v. 72, no. 11, p. 1633-1642, https://doi.org/10.1130/0016-7606(1961)72[1633:POAEOB]2.0.CO;2.","productDescription":"10 p.","startPage":"1633","endPage":"1642","costCenters":[],"links":[{"id":385864,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","otherGeospatial":"Douglas Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -113.06510925292969,\n 46.584350070440536\n ],\n [\n -112.91130065917969,\n 46.584350070440536\n ],\n [\n -112.91130065917969,\n 46.62963563393178\n ],\n [\n -113.06510925292969,\n 46.62963563393178\n ],\n [\n -113.06510925292969,\n 46.584350070440536\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Konizeski, Richard L.","contributorId":80248,"corporation":false,"usgs":true,"family":"Konizeski","given":"Richard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":816283,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220634,"text":"70220634 - 1961 - An aeromagnetic profile from anchorage to Nome, Alaska","interactions":[],"lastModifiedDate":"2021-05-21T17:35:10.663879","indexId":"70220634","displayToPublicDate":"1961-12-31T12:31:47","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"An aeromagnetic profile from anchorage to Nome, Alaska","docAbstract":"A total-intensity profile was obtained on a 500-mile flight by a U. S. Geological Survey airplane from Anchorage to Nome, Alaska, on May 4, 1954. The average flight altitude was 6,000 ft above sea level except over the Alaska Range where the flight altitude was 9,000 ft. This profile crossed eight of the major tectonic elements of Alaska at right angles to their trend and gives valuable regional information in an area where other geophysical and geological information is scarce or lacking. The profile has a net gradient downward to the northwest, most of which is ascribed to the component of the earth's main magnetic field along the flight traverse. The great variety of magnetic anomalies which are superimposed on this gradient originate from variations in lithology along the traverse. All the magnetic anomalies, except a large one over the Yukon River, are caused by magnetic rocks at or near the surface. The magnetic profile may be divided into four major segments and nine subsegments, each having a characteristic magnetic pattern. Most of these can be related to a tectonic unit. The large plutons of the Talkeetna geanticline are clearly defined by a group of anomalies having the highest amplitudes of any on the profile. The Matanuska geosyncline to the east is represented by a 25-mile section of sloping profile consistent with a thick sedimentary section but indicating that the geosyncline is comparatively narrow near Anchorage. The 200-mile central magnetic segment is relatively free from all but very minor anomalies. This segment includes the Alaska Range geosyncline, the Tanana geanticline, and the Kuskokwim geosyncline; showing only slight magnetic contrasts between each of these elements. The two geosynclines either have thick Mesozoic sedimentary sections or have underlying crystalline rocks which are low in magnetic susceptibility at shallow depths. The rocks of the geanticline have a low but not negligible magnetic susceptibility and are predominantly Paleozoic sedimentary rocks. A single 300-gamma anomaly on the west edge of the central segment is caused by a small, mafic intrusive body in the Paleozoic metamorphic rocks of Mt. Hurst. West of this anomaly the profile consists of a series of small sharp anomalies which are probably caused by Paleozoic metavolcanic rocks of the Ruby geanticline. The second largest anomaly on the profile is in the Koyukuk geosyncline over the Yukon River. The source is calculated to be more than a mile deep and may be an intrusive body at least 15 miles wide. This anomaly is flanked by 20-mile sections of flat or sloping profile which indicate areas of thick sedimentary rocks, particularly in the region west of the Yukon River. The 150-mile Norton Sound magnetic segment on the western end of the profile consists of many closely spaced anomalies produced by rocks which are either volcanic or similar to the Seward complex. Of the four Cenozoic basins or lowlands crossed by the profile, three are underlain by rocks of moderate to high magnetic susceptibility at shallow depths. These are the Cook Inlet basin, part of which overlaps rocks of the Talkeetna geanticline, the Innoko basin of central Alaska which overlies the rocks of the Ruby geanticline, and the Norton basin, in which sedimentary deposits are thin or absent. The fourth, the Minchumina basin, is underlain by the low-susceptibility rocks at the Tanana geanticline, which are also probably close to the surface.
","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1438945","usgsCitation":"King, E.R., 1961, An aeromagnetic profile from anchorage to Nome, Alaska: Geophysics, v. 26, no. 6, p. 716-726, https://doi.org/10.1190/1.1438945.","productDescription":"11 p.","startPage":"716","endPage":"726","costCenters":[],"links":[{"id":385854,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","city":"Nome","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -166.46484375,\n 63.97596090918338\n ],\n [\n -163.740234375,\n 63.97596090918338\n ],\n [\n -163.740234375,\n 65.10914820386473\n ],\n [\n -166.46484375,\n 65.10914820386473\n ],\n [\n -166.46484375,\n 63.97596090918338\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"26","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"King, E. R.","contributorId":93482,"corporation":false,"usgs":true,"family":"King","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":816264,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220631,"text":"70220631 - 1961 - Origin and development of the Three Forks Basin, Montana","interactions":[],"lastModifiedDate":"2021-05-21T17:04:12.208306","indexId":"70220631","displayToPublicDate":"1961-12-31T11:50:04","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Origin and development of the Three Forks Basin, Montana","docAbstract":"The Three Forks Basin sprawls where the intricately deformed sedimentary and volcanic rocks of the Disturbed Belt along the Rocky Mountain front are faulted against the Precambrian metamorphic rocks that make the core of the Tobacco Root, Madison, Gallatin, and Beartooth ranges. Its eastern edge is linear, controlled by steep faults at the west front of the Bridger Range. All other boundaries are sinuous and show little sign of structural control. Tertiary deposits in the basin, rich in contemporaneous rhyolitic and latitic ash, are about equally of lake, bolson, and stream origin. The western part of the basin is dominated by moderately folded Eocene and lower Oligocene rocks, more than 2000 feet thick. They dip eastward beneath apparently unfolded upper Miocene and Pliocene rocks, more than 1300 feet thick, that also dip gently eastward to the basin edge. Thin but extensive Quaternary deposits lying unconformably on the Tertiary and pre-Tertiary rocks are mainly of rounded terrace and flood-plain gravel, angular fan gravel, and wind-blown silt. The basin began as part of an east-flowing stream system that developed in Late Cretaceous and Paleocene time, concurrently with Laramide folding and thrusting; the faulted contact between metamorphic and sedimentary rocks was especially erodible and became a main drainage way. Recurrent uplift to the west throughout the Tertiary provided gradient and load to the streams; additional load was provided by showers of ash from unknown vents. Relative uplifts of the Bridger Range in Eocene and early Oligocene time, and again in late Miocene and Pliocene time, impeded flow from the basin and led to deposits in channels, flood plains, and lakes. During most of Oligocene and Miocene time, however, the basin was being eroded. By the end of the Tertiary the basin was deeply filled and became part of a regional surface of low relief. Regional northwestward tilting stimulated headward erosion of the Missouri River which then captured the formerly east-draining or closed basin. The Tertiary deposits have been deeply eroded, and the rugged pre-basin surface partly exhumed.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1003:OADOTT]2.0.CO;2","usgsCitation":"Robinson, G.D., 1961, Origin and development of the Three Forks Basin, Montana: Bulletin of the Geological Society of America, v. 72, no. 7, p. 1303-1313, https://doi.org/10.1130/0016-7606(1961)72[1003:OADOTT]2.0.CO;2.","productDescription":"11 p.","startPage":"1303","endPage":"1313","costCenters":[],"links":[{"id":385851,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","city":"Three Forks","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.7913818359375,\n 45.80391388619765\n ],\n [\n -111.37115478515625,\n 45.80391388619765\n ],\n [\n -111.37115478515625,\n 46.02938880791639\n ],\n [\n -111.7913818359375,\n 46.02938880791639\n ],\n [\n -111.7913818359375,\n 45.80391388619765\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Robinson, G. D.","contributorId":96669,"corporation":false,"usgs":true,"family":"Robinson","given":"G.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":816261,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220602,"text":"70220602 - 1961 - Sandstone-type uranium deposits at Ambrosia Lake, New Mexico-An interim report","interactions":[],"lastModifiedDate":"2021-05-21T14:30:00.203583","indexId":"70220602","displayToPublicDate":"1961-11-01T16:44:43","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Sandstone-type uranium deposits at Ambrosia Lake, New Mexico-An interim report","docAbstract":"The Ambrosia Lake district in northwestern New Mexico is the most important uranium mining and milling district in the United States. Together with the nearby Laguna district it contains more than 50 percent of the nation's reserves.Most of the ore occurs in the Morrison formation of Late Jurassic age as elongate, tabular, mantolike bodies principally in the upper half of the Westwater Canyon sandstone member and near the base of the Poison Canyon sandstone tongue (9). Individual deposits are distributed along two easterly trending belts 2 to 3 miles apart. The ore bodies are as much as 3,000 feet long, several hundred feet wide, and 100 feet thick. Depths to the ore range from 0 to 2,200 feet. Some ore is also mined from the Todilto limestone of Late Jurassic age and from the Dakota sandstone of Early (?) and Late Cretaceous age.Two types of unoxidized ore are recognized: prefault ore, which is considered to be primary, and postfault ore, which may be redistributed. The prefault ore shows no obvious relationship to tectonic structures but appears to be controlled by a variety of sedimentary structures. Postfault ore is controlled by a combination of sedimentary and tectonic structures. Disseminated carbonaceous matter, believed to be plant derived, appears to be the dominant control in the localization of the uranium.The ore mineralogy is comparatively simple, and coffinite is by far the most abundant ore mineral. Molybdenum, selenium, vanadium, and iron occur in anomalous quantities in the deposits in both oxidized and unoxidized minerals.U/eU ratios and radioisotope distribution indicate almost universal disequilibrium and fairly recent migration of radioisotopes in all deposits that have been sampled.Further studies on the organic carbonaceous matter, sandstone alteration, age determinations, and sulfur isotope composition are required to obtain a better understanding of the source, transportation, and deposition of uranium and other elements in the deposits.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.56.7.1179","usgsCitation":"Granger, H., Santos, E., Dean, B., and Moore, F.B., 1961, Sandstone-type uranium deposits at Ambrosia Lake, New Mexico-An interim report: Economic Geology, v. 56, no. 7, p. 1179-1210, https://doi.org/10.2113/gsecongeo.56.7.1179.","productDescription":"32 p.","startPage":"1179","endPage":"1210","costCenters":[],"links":[{"id":385818,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Ambrosia Lake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -107.962646484375,\n 35.11990857099681\n ],\n [\n -107.5286865234375,\n 35.11990857099681\n ],\n [\n -107.5286865234375,\n 35.61711648382185\n ],\n [\n -107.962646484375,\n 35.61711648382185\n ],\n [\n -107.962646484375,\n 35.11990857099681\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"56","issue":"7","noUsgsAuthors":false,"publicationDate":"1961-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Granger, H.C.","contributorId":15203,"corporation":false,"usgs":true,"family":"Granger","given":"H.C.","email":"","affiliations":[],"preferred":false,"id":816126,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Santos, E.S.","contributorId":95883,"corporation":false,"usgs":true,"family":"Santos","given":"E.S.","email":"","affiliations":[],"preferred":false,"id":816127,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dean, B.G.","contributorId":18845,"corporation":false,"usgs":true,"family":"Dean","given":"B.G.","email":"","affiliations":[],"preferred":false,"id":816128,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Moore, F. B.","contributorId":12461,"corporation":false,"usgs":true,"family":"Moore","given":"F.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":816129,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70220628,"text":"70220628 - 1961 - Granitic formations in the east-central Sierra Nevada near Bishop, California","interactions":[],"lastModifiedDate":"2021-05-21T16:24:18.750243","indexId":"70220628","displayToPublicDate":"1961-10-01T11:17:15","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Granitic formations in the east-central Sierra Nevada near Bishop, California","docAbstract":"This report establishes lithologic units among the granitic rocks of the east-central Sierra Nevada near Bishop, California. In this area the Sierra Nevada batholith is composed chiefly of quartz-bearing plutonic rocks ranging in composition from quartz diorite to alaskite but includes scattered small masses of darker and older plutonic rocks and remnants of metamorphosed sedimentary and volcanic rocks. The granitic rocks are in discrete plutons, either in sharp contact with one another or separated by thin septa of metamorphic or mafic igneous rock or by late aplitic dikes. The granitic rocks are grouped into lithologic units on the basis of composition, texture, and intrusive relations. The units include six new formations, three informal units made up of the rocks in several plutons, and four informal units that include the rocks in single plutons. The new formations are the Inconsolable Granodiorite, Tinemaha Granodiorite, Wheeler Crest Quartz Monzonite, Round Valley Peak Granodiorite, Lamarck Granodiorite, and Tungsten Hills Quartz Monzonite.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1521:GFITES]2.0.CO;2","usgsCitation":"Bateman, P.C., 1961, Granitic formations in the east-central Sierra Nevada near Bishop, California: Bulletin of the Geological Society of America, v. 72, no. 10, p. 1521-1537, https://doi.org/10.1130/0016-7606(1961)72[1521:GFITES]2.0.CO;2.","productDescription":"17 p.","startPage":"1521","endPage":"1537","costCenters":[],"links":[{"id":385848,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Bishop","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.60290527343749,\n 37.13842453422676\n ],\n [\n -117.9766845703125,\n 37.13842453422676\n ],\n [\n -117.9766845703125,\n 37.501010429493284\n ],\n [\n -118.60290527343749,\n 37.501010429493284\n ],\n [\n -118.60290527343749,\n 37.13842453422676\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bateman, Paul C.","contributorId":18377,"corporation":false,"usgs":true,"family":"Bateman","given":"Paul","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":816256,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70190790,"text":"70190790 - 1961 - Records and water-level measurements of selected wells and chemical analysis of ground water, East Shore area, Davis, Weber, and Box Elder Counties","interactions":[],"lastModifiedDate":"2017-09-14T10:52:08","indexId":"70190790","displayToPublicDate":"1961-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5497,"text":"Utah Basic-Data Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"1","title":"Records and water-level measurements of selected wells and chemical analysis of ground water, East Shore area, Davis, Weber, and Box Elder Counties","docAbstract":"This report is intended to serve two purposes: (1) to make available to the public basic ground-water data useful in planning and studying development of water resources and (2) to supplement an interpretive report that will be published later.
Records were collected during the period 1935-61 by the U.S. Geological Survey in cooperation with the Utah State Engineer as a part of the investigation of the ground-water resources of the East Shore area in Davis, Weber, and southern Box Elder Counties, Utah. During the period 1952-61 additional records were collected by the U.S. Bureau of Reclamation. The interpretive material will be published cooperatively by the U.S. Geological Survey and the Utah State Engineer as a report entitled \"Groundwater conditions in the East Shore area, Utah, 1953-61,\" by Ralph E. Smith.
This report is most useful in predicting conditions likely to be found in areas that are being considered as well sites. The person considering the new well can spot the proposed site on plate 1 and examine the records of nearby wells as shown on the tables and figures. From table 1 he can note (1) the depth and diameter of wells in the vicinity and the yield of some of those wells, and (2) the depth to water or the feet of water pressure in wells in the vicinity; from table 2 and figure 2 he may note the historic fluctuations and trends of water levels in the vicinity; and from tables 3 and l he may note the chemical quality of the water from wells in the vicinity and the use made of this water. If the reader decides from his examination that conditions are favorable, he may place an application to drill a well with the State Engineer. If the State Engineer believes unappropriated water is available, the application may be approved after minimum statutory requirements have been satisfied.
The report is also useful when planning large-scale developments of water supply. This and other uses of the report will be helped by use of the interpretive report upon its release.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared in cooperation with the Utah State Engineer's Office","usgsCitation":"Smith, R., 1961, Records and water-level measurements of selected wells and chemical analysis of ground water, East Shore area, Davis, Weber, and Box Elder Counties: Utah Basic-Data Report 1, 35 p.","productDescription":"35 p.","numberOfPages":"40","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":345752,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":345751,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.waterrights.utah.gov/cgi-bin/docview.exe?Folder=TP21-1-020&Title=Basic+Data+Report+1"}],"country":"United States","state":"Utah","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"59bb953ce4b091459a578240","contributors":{"authors":[{"text":"Smith, Ralph E.","contributorId":178301,"corporation":false,"usgs":true,"family":"Smith","given":"Ralph E.","affiliations":[],"preferred":false,"id":710414,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70174095,"text":"70174095 - 1961 - Geology and ground-water resources of Clayton County, Iowa","interactions":[],"lastModifiedDate":"2025-07-30T13:18:13.21876","indexId":"70174095","displayToPublicDate":"1961-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":148,"text":"Water Supply Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"7","title":"Geology and ground-water resources of Clayton County, Iowa","docAbstract":"Clayton County includes 784 square miles in northeastern Iowa and in 1960 had a population of 21, 962. For the most part, the county is a dissected upland that is drained mainly by the southeastward flowing Turkey River and its principal tributary, the Volga River. The Turkey River empties into the Mississippi River, which flows southward along the eastern border of the county. The climate is humid continental, and the average annual precipitation is 33.01 inches. The economy of the county is based on farming and the raising of livestock. The natural resources of the county include soil, water, rock, sand, and timber.
","language":"English","publisher":"State of Iowa","publisherLocation":"Des Moines, IA","usgsCitation":"Steinhilber, W.L., Van Eck, O.J., and Feulner, A., 1961, Geology and ground-water resources of Clayton County, Iowa: Water Supply Bulletin 7, xi, 142 p.","productDescription":"xi, 142 p.","numberOfPages":"154","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":493175,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70174095/IGS_wsb_7.pdf","text":"Report","size":"13.5 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":324470,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Iowa","county":"Clayton County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-91.604,43.0816],[-91.4892,43.0817],[-91.37,43.0807],[-91.2546,43.0802],[-91.1944,43.08],[-91.178,43.0798],[-91.1777,43.0732],[-91.1782,43.0655],[-91.1776,43.0584],[-91.1766,43.0506],[-91.1756,43.0415],[-91.1716,43.0291],[-91.1677,43.0192],[-91.1624,43.0071],[-91.1589,42.9989],[-91.1579,42.9966],[-91.1566,42.9934],[-91.1563,42.9894],[-91.1568,42.9839],[-91.1585,42.9784],[-91.1566,42.9747],[-91.1559,42.9739],[-91.152,42.9695],[-91.1506,42.9678],[-91.1464,42.9609],[-91.1455,42.9518],[-91.1457,42.9445],[-91.1454,42.9395],[-91.1453,42.9372],[-91.1438,42.9268],[-91.1445,42.9168],[-91.1444,42.9104],[-91.1411,42.905],[-91.1372,42.9007],[-91.1311,42.8965],[-91.1218,42.8927],[-91.1132,42.8885],[-91.1047,42.8824],[-91.0999,42.875],[-91.0995,42.874],[-91.0971,42.8678],[-91.0944,42.8596],[-91.0924,42.8542],[-91.0908,42.8498],[-91.089,42.8462],[-91.086,42.8443],[-91.0847,42.8437],[-91.0823,42.8424],[-91.0796,42.8398],[-91.0775,42.8373],[-91.0776,42.8339],[-91.0781,42.8294],[-91.078,42.8214],[-91.0776,42.8103],[-91.0763,42.8],[-91.0735,42.7913],[-91.0713,42.7826],[-91.0696,42.7771],[-91.0688,42.7736],[-91.0667,42.7698],[-91.0649,42.767],[-91.0629,42.7645],[-91.062,42.762],[-91.0621,42.7591],[-91.0634,42.7561],[-91.0639,42.7545],[-91.0638,42.754],[-91.0632,42.7523],[-91.0613,42.75],[-91.0587,42.7487],[-91.0582,42.7485],[-91.0563,42.7478],[-91.0549,42.746],[-91.0549,42.7446],[-91.0543,42.7428],[-91.0517,42.7397],[-91.0492,42.7383],[-91.0467,42.7379],[-91.0447,42.7376],[-91.0417,42.7375],[-91.0392,42.7375],[-91.0354,42.7371],[-91.0323,42.7358],[-91.0305,42.7341],[-91.03,42.7314],[-91.0301,42.7291],[-91.0283,42.7263],[-91.0264,42.7249],[-91.0259,42.7245],[-91.0226,42.7227],[-91.0182,42.7205],[-91.0075,42.7161],[-90.998,42.7121],[-90.9903,42.7074],[-90.9841,42.7036],[-90.98,42.6995],[-90.9734,42.6956],[-90.9677,42.6929],[-90.9601,42.6898],[-90.9542,42.6872],[-90.9482,42.6858],[-90.9413,42.685],[-90.9382,42.685],[-90.9332,42.6856],[-90.9276,42.6856],[-90.9226,42.6843],[-90.9169,42.6821],[-90.9108,42.68],[-90.9065,42.6785],[-90.8985,42.6761],[-90.896,42.6753],[-90.8962,42.6697],[-90.8978,42.6447],[-91.0181,42.6452],[-91.1334,42.6451],[-91.2519,42.6445],[-91.3691,42.6437],[-91.4876,42.6442],[-91.606,42.6437],[-91.6055,42.731],[-91.605,42.8169],[-91.6045,42.9056],[-91.6046,42.9915],[-91.604,43.0816]]]},\"properties\":{\"name\":\"Clayton\",\"state\":\"IA\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57724e30e4b07657d1a81983","contributors":{"authors":[{"text":"Steinhilber, W. L.","contributorId":79456,"corporation":false,"usgs":true,"family":"Steinhilber","given":"W.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":640872,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Van Eck, O. J.","contributorId":172476,"corporation":false,"usgs":false,"family":"Van Eck","given":"O.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":640873,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Feulner, A.J.","contributorId":70796,"corporation":false,"usgs":true,"family":"Feulner","given":"A.J.","affiliations":[],"preferred":false,"id":640874,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":47379,"text":"b1082E - 1960 - Strategic graphite, a survey","interactions":[{"subject":{"id":47379,"text":"b1082E - 1960 - Strategic graphite, a survey","indexId":"b1082E","publicationYear":"1960","noYear":false,"chapter":"E","title":"Strategic graphite, a survey"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":1}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T14:11:14","indexId":"b1082E","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"E","title":"Strategic graphite, a survey","docAbstract":"Strategic graphite consists of certain grades of lump and flake graphite for which the United States is largely or entirely dependent on sources abroad. Lump graphite of high purity, necessary in the manufacture of carbon brushes, is imported from Ceylon, where it occurs in vein deposits. Flake graphite, obtained from deposits consisting of graphite disseminated in schists and other metamorphic rocks, is an essential ingredient of crucibles used in the nonferrous metal industries and in the manufacture of lubricants and packings. High-quality flake graphite for these uses has been obtained mostly from Madagascar since World War I. Some flake graphite of strategic grade has been produced, however, from deposits in Texas, Alabama, and Pennsylvania. The development of the carbon-bonded crucible, which does not require coarse flake, should lessen the competitive advantage of the Madagascar producers of crucible flake.
Graphite of various grades has been produced intermittently in the United States since 1644. The principal domestic deposits of flake graphite are in Texas, Alabama, Pennsylvania, and New York. Reserves of flake graphite in these four States are very large, but production has been sporadic and on the whole unprofitable since World War I, owing principally to competition from producers in Madagascar. Deposits in Madagascar are large and relatively high in content of flake graphite. Production costs are low and the flake produced is of high quality. Coarseness of flake and uniformity of the graphite products marketed are cited as major advantages of Madagascar flake. In addition, the usability of Madagascar flake for various purposes has been thoroughly demonstrated, whereas the usability of domestic flake for strategic purposes is still in question.
Domestic graphite deposits are of five kinds: deposits consisting of graphite disseminated in metamorphosed siliceous sediments, deposits consisting of graphite disseminated in marble, deposits formed by thermal or dynamothermal metamorphism of coal beds or other highly carbonaceous sediments, vein deposits, and contact metasomatic deposits in marble. Only the first kind comprises deposits sufficiently large and rich in flake graphite to be significant potential sources of strategic grades of graphite. Vein deposits in several localities are known, but none is known to contain substantial reserves of graphite of strategic quality.
Large resources of flake graphite exist in central Texas, in northeastern Alabama, in eastern Pennsylvania, and in the eastern Adirondack Mountains of New York. Tonnages available, compared with the tonnages of flake graphite consumed annually in the United States, are very large. There have been indications that flake graphite from Texas, Alabama, and Pennsylvania can be used in clay-graphite crucibles as a substitute for Madagascar flake, and one producer has made progress in establishing markets for his flake products as ingredients of lubricants. The tonnages of various commercial grades of graphite recoverable from various domestic deposits, however, have not been established; hence, the adequacy of domestic resources of graphite in a time of emergency is not known.
The only vein deposits from which significant quantities of lump graphite have been produced are those of the Crystal Graphite mine, Beaverhead County, Mont. The deposits are fracture fillings in Precambrian gneiss and pegmatite. Known reserves in the deposits are small.
In Texas, numerous flake-graphite deposits occur in the Precambrian Packsaddle schist in Llano and Burnet Counties. Graphite disseminated in certain parts of this formation ranges from extremely fine to medium grained. The principal producer has been the mine of the Southwestern Graphite Co., west of the town of Burnet. Substantial reserves of medium-grained graphite are present in the deposit mined by the company.
In northeastern Alabama, flake-graphite deposits occur in the Ashland mica schist in two belts that trend northeastward across Clay, Goosa, and Chilton Counties. The northeastern belt has been the most productive. About 40 mines have been operated at one time or another, but only a few have been active during or since World War I. The deposits consist of flake graphite disseminated in certain zones or \"leads\" consisting of quartz-mica-feldspar schists and mica quartzite. Most of past production has come from the weathered upper parts of the deposits, but unweathered rock has been mined at several localities. Reserves of weathered rock containing 3 to 5 percent graphite are very large, and reserves of unweathered rock are even greater.
Flake graphite deposits in Chester County, Pa., have been worked intermittently since about 1890. The deposits consist of medium- to coarse-grained graphite disseminated in certain belts of the Pickering gneiss. The most promising deposit is one worked in the Benjamin Franklin and the Eynon Just mines. Reserves of weathered rock containing 1.5 percent graphite are of moderate size; reserves of unweathered rock are large.
In the eastern Adirondack Mountains in New York there are two principal kinds of flake-graphite deposits: contact-metasomatic deposits and those consisting of flake graphite disseminated in quartz schist. The contact-metasomatic deposits are small, irregular, and very erratic in graphite content. The deposits in quartz schist are very large, persistent, and uniform in grade. There are large reserves of schist containing 3 to 5 percent graphite, but the graphite is relatively fine grained.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082E","usgsCitation":"Cameron, E.N., and Weis, P., 1960, Strategic graphite, a survey: U.S. Geological Survey Bulletin 1082, Report: v, 120 p.; 4 Plates: 30.56 x 27.81 inches or smaller, https://doi.org/10.3133/b1082E.","productDescription":"Report: v, 120 p.; 4 Plates: 30.56 x 27.81 inches or smaller","startPage":"201","endPage":"321","costCenters":[],"links":[{"id":100004,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082e/plate-10.pdf","text":"Plate 10","size":"322 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 10"},{"id":100002,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082e/plate-08.pdf","text":"Plate 8","size":"743 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 8"},{"id":100003,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082e/plate-09.pdf","text":"Plate 9","size":"236 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 9"},{"id":100005,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082e/plate-11.pdf","text":"Plate 11","size":"525 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 11"},{"id":170745,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082e/report-thumb.jpg"},{"id":100001,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082e/report.pdf","text":"Report","size":"8.79 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b28e4b07f02db6b1369","contributors":{"authors":[{"text":"Cameron, Eugene N.","contributorId":59498,"corporation":false,"usgs":true,"family":"Cameron","given":"Eugene","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":235185,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weis, Paul L.","contributorId":102872,"corporation":false,"usgs":true,"family":"Weis","given":"Paul L.","affiliations":[],"preferred":false,"id":235186,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":64309,"text":"gp235 - 1960 - Aeromagnetic map of part of the Easton quadrangle, Northampton County, Pennsylvania, and Warren County, New Jersey","interactions":[],"lastModifiedDate":"2021-12-08T19:56:03.249037","indexId":"gp235","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"235","title":"Aeromagnetic map of part of the Easton quadrangle, Northampton County, Pennsylvania, and Warren County, New Jersey","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp235","usgsCitation":"Bromery, R.W., Henderson, J.R., and Zandle, G.L., 1960, Aeromagnetic map of part of the Easton quadrangle, Northampton County, Pennsylvania, and Warren County, New Jersey: U.S. Geological Survey Geophysical Investigations Map 235, 1 Plate: 23.22 × 27.62 inches, https://doi.org/10.3133/gp235.","productDescription":"1 Plate: 23.22 × 27.62 inches","costCenters":[],"links":[{"id":392639,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_3157.htm"},{"id":254338,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0235/report-thumb.jpg"},{"id":250941,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0235/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":250940,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0235/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"New Jersey, Pennsylvania","county":"Northampton County, Warren County","otherGeospatial":"Easton quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.25,40.625 ], [ -75.25,40.75 ], [ -75.125,40.75 ], [ -75.125,40.625 ], [ -75.25,40.625 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae4e4b07f02db689ddb","contributors":{"authors":[{"text":"Bromery, Randolph Wilson","contributorId":22746,"corporation":false,"usgs":true,"family":"Bromery","given":"Randolph","email":"","middleInitial":"Wilson","affiliations":[],"preferred":false,"id":270520,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Henderson, J. R. Jr.","contributorId":88802,"corporation":false,"usgs":true,"family":"Henderson","given":"J.","suffix":"Jr.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":270522,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Zandle, G. L.","contributorId":39863,"corporation":false,"usgs":true,"family":"Zandle","given":"G.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":270521,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":47383,"text":"b1082I - 1960 - Geology and mineral deposits of the St. Regis-Superior area, Mineral County, Montana","interactions":[{"subject":{"id":42851,"text":"ofr5621 - 1956 - Reconnaissance geologic map of the St. Regis-Superior area, Mineral County, Montana","indexId":"ofr5621","publicationYear":"1956","noYear":false,"title":"Reconnaissance geologic map of the St. Regis-Superior area, Mineral County, Montana"},"predicate":"SUPERSEDED_BY","object":{"id":47383,"text":"b1082I - 1960 - Geology and mineral deposits of the St. Regis-Superior area, Mineral County, Montana","indexId":"b1082I","publicationYear":"1960","noYear":false,"chapter":"I","title":"Geology and mineral deposits of the St. Regis-Superior area, Mineral County, Montana"},"id":1},{"subject":{"id":47383,"text":"b1082I - 1960 - Geology and mineral deposits of the St. Regis-Superior area, Mineral County, Montana","indexId":"b1082I","publicationYear":"1960","noYear":false,"chapter":"I","title":"Geology and mineral deposits of the St. Regis-Superior area, Mineral County, Montana"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":2}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2023-03-08T22:21:15.346782","indexId":"b1082I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"I","title":"Geology and mineral deposits of the St. Regis-Superior area, Mineral County, Montana","docAbstract":"The St. Regis-Superior area occupies about 300 square miles in northwestern Montana and includes parts of the Squaw Peak Range and Coeur d'Alerie Mountains of the northern Rocky Mountains physiographic province. Nearly 50,000 feet of metasedimentary rocks of the Precambrian Belt series, chiefly varieties of quartzite and argillite, underlies most of the area. The Belt series is informally subdivided with reference to the top of the Wallace formation into lower and upper parts. In this area, the lower part of the Belt series is divided into the Prichard, Burke and Revett, St. Regis, and Wallace formations, in order of decreasing age, and the upper part of the Belt series or the Missoula group is divided »into the Spruce, Lupine, Sloway, and Bouchard formations, and an unnamed feldspathic quartzite at Rock Rabbit Ridge, also from oldest to youngest. Formations in the lower part of the Belt series are correlated with formations of the same names in the Coeur d'Alene district, and formations in the upper part of the Belt series are tentatively correlated in part with formations of the Missoula group in the vicinity of Missoula, Mont. Paleozoic quartzite, shale, limestone, and dolomite crop out in several localities in the southeastern part of the area. The limestone unit contains fragments of a single species of Glossopleura of early Middle Cambrian age which, together with lithologic similarities, has been used to correlate at least the quartzite, shale, and limestone part of this Paleozoic sequence with the Flathead sandstone, Gordon shale, and Damnation limestone sequence known elsewhere in northwestern Montana. Several small diabasic dikes and sills are present in the area, generally associated with northwestward-trending faults.
The major faults generally trend northwestward and are considered to be part of the Lewis and Clark structural line. The Osburn fault, the major element of the Lewis and Clark line through the Coeur d'Alene district and western Mineral County, has been traced to the east edge of the St. Regis- Superior area, thus extending the mapped length of the fault to about 100 miles. Evidence indicates that this major fault has diminished in intensity in this area and that most of the stress has been relieved along the Boyd Mountain fault that apparently splits from the Osburn fault a few miles west of St. Regis. Stratigraphic and structural evidence indicates a strike-slip right-lateral movement of about 3 miles along the Osburn fault. Horizontal stratigraphic separation along the Boyd Mountain fault indicates a right-lateral movement of about 13 miles.
Low-grade regional metamorphism of the sedimentary rocks in the area has caused the recrystallization of quartz grains and the formation of sericite. Argillite and quartzite have been converted to phyllite and foliated quartzite by dynamic metamorphism in a large area north of the central part of the Osburn fault. Some of the shear zones contain a large amount of introduced carbonate minerals.
From 1901 through 1953 this area has produced 8,086,827 pounds of zinc, 7,932,958 pounds of lead, 2,053,715 pounds of copper, 584,168 fine ounces of silver, and 588 fine ounces of gold. The lead, sine, and silver have come chiefly from veins in highly foliated rocks near the Osburn fault zone. The attitudes of these veins are controlled in large part by the cleavage. The principal ore minerals are galena, sphalerite, tetrahedrite, and boulangerite, and the gangue minerals are quartz, carbonate minerals, and barite. Most of the copper has come from the Amador vein where chalcopyrite and bornite are the principal ore minerals, and the gangue minerals are pyrite, quartz, and carbonate minerals. The Amador vein occurs in a belt of copper deposits that extends westward into the Coeur d'Alene district. These copper deposits may be genetically associated with diorite dikes and sills lying within the same belt.
Fluorspar has been found in three closely spaced prospects along a northward- trending zone of brecciation and small-scale folding in Dry Creek valley. Incomplete production records show that 781 tons of fluorspar has been shipped from 2 of these prospects.
The fluorspar deposits in the Northgate district, Jackson County, Colo., are among the largest in Western United States. The mines were operated intermittently during the 1920's and again during World War II, but production during these early periods of operation was not large. Mining was begun on a larger scale in 1951, and the district has assumed a prominent position among the fluorspar producers in the United States.
Within the Northgate district, Precambrian metamorphic and igneous rocks crop out largely in the Medicine Bow Mountains, and later sedimentary rocks underlie North Park and fill old stream valleys in the mountains.
The metamorphic rocks constitute a gneiss complex that formed under progressively changing conditions of regional metamorphism. They consist principally of hornblende-plagioclase gneiss (hornblende gneiss), quartz monzonite gneiss, pegmatite, biotite-garnet-quartz-plagioclase gneiss (biotite-garnet gneiss), hornblende-biotite-quartz-plagioclase gneiss (hornblende-biotite gneiss) and mylonite gneiss.
The igneous rocks comprise some local fine-grained dacite porphyry dikes near the west margin of the district, and a quartz monzonitic stock and associated dikes in the central and eastern parts of the district.
The sedimentary rocks in the district range in age from Permian to Recent. Folded Permian and Mesozoic rocks underlie the basin of North Park, and consist in sequence from oldest to youngest, of Satanka(?) shale (0-50 feet of brick-red shale) and Forelle(?) limestone (8-15 feet of pink to light-gray laminated limestone) of Permian age, Chugwater formation of Permian and Triassic age (690 feet of red silty shale and sandstone), Sundance formation of Late Jurassic age (145 feet of sandstone containing some shale and limestone), Morrison formation of Late Jurassic age (445 feet of variegated shale and minor sandstone and limestone), Dakota group as used by Lee (1927), now considered to be of Early Cretaceous age in this area (200-320 feet of pebbly sandstone, sandstone, and shale), Ben ton shale of Early and Late Cretaceous age (665 feet of dark-gray thin-bedded shale), Niobrara formation of Late Cretaceous age (865 feet of yellow to gray limy siltstone and shale), and Pierre shale of Late Cretaceous age (more than 60 feet of dark-gray fissile shale). Unconformities separate the Chugwater and Sundance formations, and the Morrison formation and the Dakota group.
Nonmarine strata of the White River formation of Oligocene age and the North Park formation of Miocene and Pliocene (?) age fill Tertiary valleys cut in the Precambrian rocks of the mountain areas, and Quaternary terrace gravel, alluvium, and dune sand mantle much of the floor of North Park.
The main outlines of the modern Rocky Mountains formed during the Laramide orogeny in late Mesozoic and early Tertiary time. Most of the Laramide structures that can be recognized in the Northgate district involve the sedimentary rocks underlying North Park which are folded into northwest-trending anticlines and synclines. The folds are open and in most the beds dip 60° or less. Yet many anticlines are cut by reverse faults of widely different trends and directions of offset. Transverse faults offset some of the folds, and the character of folding commonly is markedly different on opposing sides of these faults. The North Park basin is cut off on the north by the east-trending Independence Mountain fault, a north-dipping reverse fault along which hard Precambrian rocks have been thrust up across the trend of the earlier Laramide structures. The North Park basin is still a major structure where it is interrupted by the Independence Mountain fault, and the original basin must have extended much farther north.
Disrupted gradients at the base of pre-White River valleys suggest that the Northgate district and adjacent areas may have been deformed in middle Tertiary time, but the evidence is not conclusive. A more definite period of deformation took place in Pliocene time following deposition of the North Park formation. North Park strata in south-central North Park were folded into a northwest-trending syncline, and the central part of the Northgate district probably was warped up along a north- or northwestward-trending axis.
Four north- to northwestward-trending faults cut the Precambrian rocks and White River formation on Pinkham Mountain and the area to the southeast. Similar faults 2½ and 15 miles west of the Northgate district cut rocks of the North Park formation, and all probably formed during the Pliocene period of deformation. The known commercial fluorspar deposits are localized along the two larger faults of the Northgate district, and they have been studied in detail.
The White River formation in early Oligocene time covered a hilly terrain drained by southward-flowing streams. By late Miocene, the northward-flowing streams had cut to about the same levels reached by the pre-White River streams and had partly exhumed and modified the older terrain. During late Miocene and early Pliocene (?) time, the Northgate area was buried beneath the clays, sands, and gravels of the North Park formation. Subsequent erosion removed the higher part of the North Park formation, cut a surface of low relief across the exhumed Precambrian rocks, and removed all topographic evidence of the Pliocene period of deformation. The present courses of the major streams were superimposed across the buried terrains during this period of erosion. Rejuvenation during middle Pleistocene caused all major streams to become incised in sharp canyons.
Copper minerals occur in small concentrations in some of the pegmatite masses in the gneiss complex. The copper-rich masses rarely exceed a few feet in diameter and constitute only a small part of the associated pegmatite body.
Vermiculite is exposed in prospect pits and mine workings along the west margin of the Northgate district. All the venniculite that was seen is associated with small masses of horablendite, massive chlorite, or serpentinite where these masses are near or are cut by pegmatite bodies. Some of the deposits may be potential producers of commercial-grade vermiculite, but most are small and erratic in shape or grade.
Fluorspar is the main mineral commodity that has been produced from the Northgate district. It was deposited during two distinct periods of mineralization, but only the younger deposits have been productive.
Small bodies of silicified breccia containing minor coarsely crystalline fluorite occur along the Independence Mountain fault, and in a few places along other Laramide faults. The fluorspar is an integral part of the fault breccia and apparently was deposited while the enclosing fault was still active.
The largest deposits of fluorspar in the Northgate district occur along the late Tertiary (?) faults on Pinkham Mountain. The fluorspar consists typically of botryoidal layers that formed as successive encrustations along open fractures, or as finely granular aggregates replacing and cementing fault gouge and White River formation. Many incompletely filled cavities, called water courses, still exist. Fluorite is the principal vein material; fragments of country rock constitute the chief impurity although finely granular quartz or chalcedony is common locally. Soft powdery manganese oxide coats many fractures and in places is associated with a fine white clay.
Fluorspar was deposited in or adjacent to open spaces along the late Tertiary (?) faults. Fractures in hard granitic rocks tended to remain open after faulting and were the favored sites for fluorspar deposition; fractures in the less competent hornblende and hornblende-biotite gneiss and schist generally were tight and little fluorspar was deposited. The White River rocks, although soft, were permeable and were widely impregnated or replaced by fluorspar.
Both of the main vein zones are along faults that have predominant rightlateral strike-slip displacement. As they theoretically should be, the vein zones are narrower and contain less fluorspar where the containing fault is deflected to the left than where the fault is deflected to the right and the fractures remained open.
The crustified, vuggy structure of the fluorspar and the common association with chalcedony or finely granular quartz suggest deposition in a very shallow environment, but no direct evidence bearing on the depth at which the fluorspar formed was seen. Fluorspar was deposited throughout a vertical range of 600 feet or more on each of the main vein zones, and for a vertical range of 1,050 feet for the district as a whole. None of the deposits had been bottomed at the time this report was prepared.
Exploration at depth beneath known ore bodies is favorable for developing large tonnages of fluorspar. The best possibilities for finding new ore bodies near the surface are along the northwestern and southeastern parts of the Fluorine-Camp Creek vein zone where large bodies of granitic rocks are intersected by the fault. These areas are generally mantled by a thick overburden, and have been inadequately tested so far.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082F","collaboration":"Prepared in cooperation with the Colorado State Geological Survey Board and the Colorado Metal Mining Fund Board","usgsCitation":"Steven, T., 1960, Geology and fluorspar deposits, Northgate district, Colorado: U.S. Geological Survey Bulletin 1082, Report: v, 99 p.; 4 Plates: 33.80 x 32.33 inches or smaller, https://doi.org/10.3133/b1082F.","productDescription":"Report: v, 99 p.; 4 Plates: 33.80 x 32.33 inches or smaller","startPage":"323","endPage":"422","costCenters":[],"links":[{"id":100010,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-15.pdf","text":"Plate 15","size":"1.58 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 15"},{"id":100007,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-12.pdf","text":"Plate 12","size":"8.26 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 12"},{"id":100008,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-13.pdf","text":"Plate 13","size":"1.27 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 13"},{"id":100009,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082f/plate-14.pdf","text":"Plate 14","size":"722 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 14"},{"id":172968,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082f/report-thumb.jpg"},{"id":109304,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20747.htm","linkFileType":{"id":5,"text":"html"},"description":"20747"},{"id":100006,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082f/report.pdf","text":"Report","size":"8.19 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Colorado","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106.33563995361328,\n 40.86965121139933\n ],\n [\n -106.19556427001953,\n 40.86965121139933\n ],\n [\n -106.19556427001953,\n 40.99855696412671\n ],\n [\n -106.33563995361328,\n 40.99855696412671\n ],\n [\n -106.33563995361328,\n 40.86965121139933\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adce4b07f02db6861aa","contributors":{"authors":[{"text":"Steven, Thomas A.","contributorId":57529,"corporation":false,"usgs":true,"family":"Steven","given":"Thomas A.","affiliations":[],"preferred":false,"id":235187,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47381,"text":"b1082G - 1960 - Areal geology of the Little Cone quadrangle, Colorado","interactions":[{"subject":{"id":47381,"text":"b1082G - 1960 - Areal geology of the Little Cone quadrangle, Colorado","indexId":"b1082G","publicationYear":"1960","noYear":false,"chapter":"G","title":"Areal geology of the Little Cone quadrangle, Colorado"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":1}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2017-10-18T14:21:27","indexId":"b1082G","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1082","chapter":"G","title":"Areal geology of the Little Cone quadrangle, Colorado","docAbstract":"The Little Cone quadrangle includes an area of about 59 square miles in eastern San Miguel County in southwestern Colorado. The quadrangle contains features characteristic of both the Colorado Plateaus physiographic province and the San Juan Mountains, and it has been affected by geologic events and processes of two different geologic environments.
The continental sedimentary rocks of the Cutler formation of Permian age are the oldest rocks exposed in the quadrangle. Deposition of the Cutler was followed by a long period of erosion and peneplanation. There is no marked angular discordance between the Cutler and the overlying Dolores formation in the Little Cone quadrangle, but there is in areas some tens of miles east and west of the quadrangle where some crustal warping took place.
The continental sedimentary rocks of the Dolores formation of Late Triassic age are red beds that are similar in gross lithology to those of the Cutler. The Dolores formation is subdivided into five general units that persist throughout the quadrangle and for some tens of miles to the north, south, and east. A second long period of erosion followed deposition of the Dolores.
The Entrada sandstone of Late Jurassic age overlies the Dolores formation, and is in turn overlain by the Wanakah formation, also of Late Jurassic age. The Wanakah consists of the Pony Express limestone member at the base, the Bilk Creek sandstone'member near the center, and a \"marl\" member at the top. The Morrison formation, which overlies the Wanakah, consists of the Salt Wash sandstone member in the lower part and the Brushy Basin shale member in the upper part. A period of erosion, probably of relatively short duration, followed deposition of the Brushy Basin member.
The Burro Canyon formation of Early Cretaceous age occurs as discontinuous bodies that fill channels cut in the top of the Morrison formation. Deposition of the Burro Canyon formation was followed by another period of erosion, which in turn ended with deposition of the Dakota sandstone of Late Cretaceous age. The Dakota sandstone grades upward into the Mancos shale, also of Late Cretaceous age.
The Paleozoic and Mesozoic formations were broadly folded during Laramide time as part of an orogeny of regional extent, and the San Juan Mountains area was uplifted as a broad dome. Extensive erosion followed deformation, and the Cretaceous rocks in the area of the Little Cone quadrangle and the Mesozoic and Paleozoic rocks eastward from the quadrangle were successively bevelled. The Telluride conglomerate of Oligocene(?) age was laid down on this surface. In the Little Cone quadrangle several hundred feet of the Telluride was deposited upon a considerable thickness (probably 3,000 feet or more) of the Mancos shale. At Telluride, about 12 miles east of the quadrangle, the Telluride conglomerate lies upon the Dolores formation. Volcanic rocks of Miocene (?) and Miocene age were deposited widely upon the Telluride conglomerate; at one time they had a thickness of probably 1,000 feet or more in the quadrangle. They have been eroded completely from the quadrangle, but are present in the San Miguel Mountains a few miles to the south and southeast.
During the middle Tertiary, probably during the Miocene, the sedimentary rocks were cut by many igneous bodies. Four major rock types are represented; in decreasing order of abundance they are granogabbro, granodidrite, rhyolite(?), and microgabbro. The granogabbro is by far the most abundant, and it forms the Flat Top Peak plug, the Little Cone laccolith, several sills in the Dakota sandstone and the Mancos shale, and a few dikes. The granodiorite forms sills in the Dakota sandstone and the Mancos shale, and the rhyolite(?) forms a single major sill in the Dakota. The microgabbro forms dikes that cut rocks as young as the Mancos shale. Metamorphic effects adjacent to the intrusive bodies generally are restricted to baking that extends only a few feet out into the enclosing rocks; in many places no metamorphic effects are evident.
The rocks in the Little Cone quadrangle were displaced along numerous faults in middle Tertiary time, probably after the igneous rocks were injected. All of the faults are normal, and have vertical or very steep dips. In part, the faults form two long and narrow northward- and northwestward-trending grabens that extend into the adjoining Placerville quadrangle to the north. The graben faults form two systems, one trending northward to northwestward, and the other trending northwestward, that are probably contemporaneous. Other faults trend eastward to northeastward; some of these appear to be related to the intrusion of the igneous rocks.
At the end of the Tertiary, probably in the early Pleistocene, the general area was again uplifted and subjected to extensive erosion. The Mancos shale was stripped from the northern part of the Little Cone quadrangle, and in this part of the area, the upland surfaces formed on top of the Dakota sandstone were largely controlled by the geologic structure.
During the Quaternary a basalt flow was erupted on Specie Mesa on a surface that cuts both the Mancos and the Dakota. The surface preserved beneath the flow has virtually the same position and slope as the adjacent present-day surfaces. Pleistocene deposits consist of (a) high-level or older drift that is unrelated to the present drainage systems and is correlated with the Cerro glacial stage of early Pleistocene age, and (b) younger drift and valley fill within the valleys of the present drainage systems that are correlated with the Durango or Wisconsin glacial stages and may represent both. Recent surficial, landslide, and spring deposits are also present.
Within the Little Cone quadrangle and in the Placerville quadrangle to the north and the Gray Head quadrangle to the east, the Entrada sandstone of Late Jurassic age contains vanadium deposits with which are associated large but low-grade amounts of uranium. These deposits form a practically continuous layer about 10 miles long and 1 to 1% miles wide, and possibly a second layer of smaller dimensions. Placer gold deposits in terrace gravel and valley fill of Pleistocene age and in alluvium of Recent age contain the only other ores.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Contributions to economic geology, 1958","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/b1082G","collaboration":"Prepared on behalf of the U.S. Atomic Energy Commission and published with the permission of the Commission","usgsCitation":"Bush, A., Marsh, O., and Taylor, R.B., 1960, Areal geology of the Little Cone quadrangle, Colorado: U.S. Geological Survey Bulletin 1082, Report: iv, 69 p.; 2 Plates: 9.44 x 13.64 inches and 26.72 x 35.00 inches, https://doi.org/10.3133/b1082G.","productDescription":"Report: iv, 69 p.; 2 Plates: 9.44 x 13.64 inches and 26.72 x 35.00 inches","startPage":"423","endPage":"492","costCenters":[],"links":[{"id":100012,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082g/plate-18.pdf","text":"Plate 18","size":"222 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 18"},{"id":100013,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082g/plate-19.pdf","text":"Plate 19","size":"7.18 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 19"},{"id":172969,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082g/report-thumb.jpg"},{"id":109305,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20748.htm","linkFileType":{"id":5,"text":"html"},"description":"20748"},{"id":100011,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082g/report.pdf","text":"Report","size":"5.24 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Colorado","county":"Miguel County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.125,\n 38\n ],\n [\n -108,\n 38\n ],\n [\n -108,\n 37.875\n ],\n [\n -108.125,\n 37.875\n ],\n [\n -108.125,\n 38\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abce4b07f02db673246","contributors":{"authors":[{"text":"Bush, A.L.","contributorId":70404,"corporation":false,"usgs":true,"family":"Bush","given":"A.L.","email":"","affiliations":[],"preferred":false,"id":235190,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Marsh, O.T.","contributorId":64672,"corporation":false,"usgs":true,"family":"Marsh","given":"O.T.","email":"","affiliations":[],"preferred":false,"id":235188,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Taylor, R. B.","contributorId":65065,"corporation":false,"usgs":true,"family":"Taylor","given":"R.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":235189,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":58398,"text":"mf230 - 1960 - Geologic and alteration maps of the East Tintic district, Utah","interactions":[],"lastModifiedDate":"2019-10-25T14:45:37","indexId":"mf230","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"230","title":"Geologic and alteration maps of the East Tintic district, Utah","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf230","usgsCitation":"Lovering, T.S., 1960, Geologic and alteration maps of the East Tintic district, Utah: U.S. Geological Survey Miscellaneous Field Studies Map 230, 2 Plates: 45.88 x 45.87 inches and 45.86 x 45.82 inches, https://doi.org/10.3133/mf230.","productDescription":"2 Plates: 45.88 x 45.87 inches and 45.86 x 45.82 inches","costCenters":[],"links":[{"id":184546,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/0230/report-thumb.jpg"},{"id":368627,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0230/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":368626,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0230/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"9600","datum":"Mean Sea Level","country":"United States","state":"Utah","otherGeospatial":"East Tintic District","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -112.08416666666666,39.916666666666664 ], [ -112.08416666666666,40 ], [ -112,40 ], [ -112,39.916666666666664 ], [ -112.08416666666666,39.916666666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8312","contributors":{"authors":[{"text":"Lovering, T. S.","contributorId":108085,"corporation":false,"usgs":true,"family":"Lovering","given":"T.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":259029,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":35305,"text":"b1072L - 1960 - Distribution of silica resources in eastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:09:35","indexId":"b1072L","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1072","chapter":"L","title":"Distribution of silica resources in eastern United States","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/b1072L","usgsCitation":"Murphy, T.D., 1960, Distribution of silica resources in eastern United States: U.S. Geological Survey Bulletin 1072, p. 657-665, ill., maps (9 fold. col. in pocket) ;24 cm., https://doi.org/10.3133/b1072L.","productDescription":"p. 657-665, ill., maps (9 fold. col. in pocket) ;24 cm.","costCenters":[],"links":[{"id":109285,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20724.htm","linkFileType":{"id":5,"text":"html"},"description":"20724"},{"id":96881,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-30.pdf","size":"514","linkFileType":{"id":1,"text":"pdf"}},{"id":96882,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-31.pdf","size":"729","linkFileType":{"id":1,"text":"pdf"}},{"id":96883,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-32.pdf","size":"823","linkFileType":{"id":1,"text":"pdf"}},{"id":96884,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-33.pdf","size":"816","linkFileType":{"id":1,"text":"pdf"}},{"id":96885,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-34.pdf","size":"741","linkFileType":{"id":1,"text":"pdf"}},{"id":96886,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-35.pdf","size":"543","linkFileType":{"id":1,"text":"pdf"}},{"id":96887,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-36.pdf","size":"610","linkFileType":{"id":1,"text":"pdf"}},{"id":96888,"rank":416,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-37.pdf","size":"301","linkFileType":{"id":1,"text":"pdf"}},{"id":96889,"rank":417,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072l/plate-38.pdf","size":"432","linkFileType":{"id":1,"text":"pdf"}},{"id":165944,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1072l/report-thumb.jpg"},{"id":63162,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1072l/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6fe4b07f02db640776","contributors":{"authors":[{"text":"Murphy, Thomas Daniel","contributorId":9322,"corporation":false,"usgs":true,"family":"Murphy","given":"Thomas","email":"","middleInitial":"Daniel","affiliations":[],"preferred":false,"id":214422,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3938,"text":"cir436 - 1960 - Preliminary report on ground water in the Salmon Falls area, Twin Falls County, Idaho","interactions":[],"lastModifiedDate":"2013-07-24T14:28:49","indexId":"cir436","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"436","title":"Preliminary report on ground water in the Salmon Falls area, Twin Falls County, Idaho","docAbstract":"The Salmon Falls area contains about 80,000 acres of irrigable land, of which about 30,000 acres receives some water from the distribution system of Salmon River Canal Co., Ltd. This system utilizes virtually all the available surface water. A substantial amount of surface water, estimated to be about 70,000 acre-feet annually, is lost by leakage from the reservoir and the distribution system. Some of this water could be salvaged by lining sections of the canal where excessive losses occur. Ground water has not been extensively developed in the area, but some successful irrigation wells furnished supplemental irrigation water. Recharge to the area is from precipitation on the area, seepage from peripheral streams, seepage losses from the reservoir and canal system, irrigation seepage, and ground-water underflow. Ground water leaves the area by undertow to the north and northwest, and eventually reaches the Snake River. The total mount of underflow from the area was estimated by three different methods to be 17,000, 100,000, and 170,000 acre-feet per year. The preliminary estimate of 100,000 acre-feet was derived by the inventory of recharge and is probably more accurate than the other two methods. Calculations, based on estimates of transmissibility computed from specific capacities of wells, suggest that there may be some channels or conduits of higher than average transmissibility through which a large part of the undertow leaves the area, Possibly 25 percent of the ground-water outflow could be intercepted by wells. However, in part of the area the depth to water may be excessive for economic development. Chemical analyses of 25 samples of ground water indicate that most of the water sampled is suitable for irrigation. The samples found least suitable were of water occurring at shallow depth, south and east of Hollister.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir436","usgsCitation":"Fowler, K.H., 1960, Preliminary report on ground water in the Salmon Falls area, Twin Falls County, Idaho: U.S. Geological Survey Circular 436, Document: iii, 17 p.; 1 Map: 14.22 x 15.24 inches, https://doi.org/10.3133/cir436.","productDescription":"Document: iii, 17 p.; 1 Map: 14.22 x 15.24 inches","numberOfPages":"21","costCenters":[],"links":[{"id":124626,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/0436/report-thumb.jpg"},{"id":31023,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/0436/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":271073,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/circ/0436/plate-1.pdf"}],"country":"United States","state":"Idaho","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -115.04,41.99 ], [ -115.04,42.9 ], [ -114.0,42.9 ], [ -114.0,41.99 ], [ -115.04,41.99 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65e11e","contributors":{"authors":[{"text":"Fowler, Kenneth H.","contributorId":23930,"corporation":false,"usgs":true,"family":"Fowler","given":"Kenneth","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":147861,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3609,"text":"cir415 - 1960 - Water management, agriculture, and ground-water supplies","interactions":[],"lastModifiedDate":"2012-02-02T00:05:34","indexId":"cir415","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"415","title":"Water management, agriculture, and ground-water supplies","docAbstract":"Encyclopedic data on world geography strikingly illustrate the drastic inequity in the distribution of the world's water supply. About 97 percent of the total volume of water is in the world's oceans. The area of continents and islands not under icecaps, glaciers, lakes, and inland seas is about 57.5 million square miles, of which 18 million (36 percent) is arid to semiarid. The total world supply of water is about 326.5 million cubic miles, of which about 317 million is in the oceans and about 9.4 million is in the land areas. Atmospheric moisture is equivalent to only about 3,100 cubic miles of water. \r\n\r\nThe available and accessible supply of ground water in the United States is somewhat more than 53,000 cubic miles (about 180 billion acre ft). The amount of fresh water on the land areas of the world at any one time is roughly 30,300 cubic miles and more than a fourth of this is in large fresh-water lakes on the North American Continent. \r\n\r\nAnnual recharge of ground water in the United States may average somewhat more than 1 billion acre-feet yearly, but the total volume of ground water in storage is equivalent to all the recharge in about the last 160 years. This accumulation of ground water is the nation's only reserve water resource, but already it is being withdrawn or mined on a large scale in a few areas. \r\n\r\nThe principal withdrawals of water in the United States are for agriculture and industry. Only 7.4 percent of agricultural land is irrigated, however; so natural soil moisture is the principal source of agricultural water, and on that basis agriculture is incomparably the largest water user. In view of current forecasts of population and industrial expansion, new commitments of water for agriculture should be scrutinized very closely, and thorough justification should be required. The 17 Western States no longer contain all the large irrigation developments. Nearly 10 percent of the irrigated area is in States east of the western bloc, chiefly in several Southeastern States. \r\n\r\nGround water is not completely 'self-renewing' because, where it is being mined, the reserve is being diminished and the reserve would be renewed only if pumping were stopped. \r\n\r\nWater is being mined at the rate of 5 million acre-feet per year in Arizona and 6 million in the High Plains of Texas. In contrast, water has been going into storage in the Snake River Plain of Idaho, where deep percolation from surface-water irrigation has added about 10 million acre-feet of storage since irrigation began. \r\n\r\nSituations in California illustrate problems of land subsidence resulting from pumping and use of water, and deterioration of ground-water reservoirs due to sea-water invasion. Much water development in the United States has been haphazard and rarely has there been integrated development of ground water and surface water. Competition is sharpening and new codes of water law are in the making. New laws, however, will not prevent the consequences of bad management. An important task for water management is to recognize the contingencies that may arise in the future and to prepare for them. \r\n\r\nThe three most important tasks at hand are to make more efficient use of water, to develop improved quantitative evaluations of water supplies arid their quality, and to develop management practices which are based on scientific hydrology.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir415","usgsCitation":"Nace, R.L., 1960, Water management, agriculture, and ground-water supplies: U.S. Geological Survey Circular 415, 12 p. :ill. ;27 cm., https://doi.org/10.3133/cir415.","productDescription":"12 p. :ill. ;27 cm.","costCenters":[],"links":[{"id":124431,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0415/report-thumb.jpg"},{"id":30645,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0415/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e478fe4b07f02db48a012","contributors":{"authors":[{"text":"Nace, Raymond L.","contributorId":93460,"corporation":false,"usgs":true,"family":"Nace","given":"Raymond","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":147251,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13876,"text":"ofr6059 - 1960 - An aeromagnetic reconnaissance of the Cook Inlet area, Alaska","interactions":[{"subject":{"id":13876,"text":"ofr6059 - 1960 - An aeromagnetic reconnaissance of the Cook Inlet area, Alaska","indexId":"ofr6059","publicationYear":"1960","noYear":false,"title":"An aeromagnetic reconnaissance of the Cook Inlet area, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":39075,"text":"pp316G - 1963 - An aeromagnetic reconnaissance of the Cook Inlet area, Alaska","indexId":"pp316G","publicationYear":"1963","noYear":false,"chapter":"G","title":"An aeromagnetic reconnaissance of the Cook Inlet area, Alaska"},"id":1}],"supersededBy":{"id":39075,"text":"pp316G - 1963 - An aeromagnetic reconnaissance of the Cook Inlet area, Alaska","indexId":"pp316G","publicationYear":"1963","noYear":false,"title":"An aeromagnetic reconnaissance of the Cook Inlet area, Alaska"},"lastModifiedDate":"2023-10-06T20:39:35.658058","indexId":"ofr6059","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-59","title":"An aeromagnetic reconnaissance of the Cook Inlet area, Alaska","docAbstract":"Forty-two east-west aeromagnetic lines were flown across the Cook Inlet-Susitna Lowland between Chelatna Lake and Seldovia at a flight altitude of approximately 2,500 feet. The lines traverse all or part of five Mesozoic tectonic elements that dominate the structure of the Cook Inlet area. Each of these tectonic elements, the Alaska Range geosyncline, the Talkeetna geanticline, the Matanuska geosyncline, the Seldovia geanticline, and the Chugach Mountains geosyncline, has a characteristic magnetic pattern.
The aeromagnetic data, compiled as total intensity aeromagnetic profiles, show several significant features which are consistent with the structural grain of the area. A two-dimensional anomaly was observed near the east edge of the area on all but the southernmost profiles, where it becomes obscure. Geologic evidence suggests that this feature, the Knik Arm anomaly, is produced by plutonic rocks that have been intruded along the Seldovia geanticline. Southeast of this anomaly the profiles are almost flat. This flatness indicates that magnetic rocks are deeply buried in this area, which is underlain by slate and graywacke deposited in the Chugach Mountains geosyncline.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6059","usgsCitation":"Grantz, A., Zietz, I., and Andreasen, G., 1960, An aeromagnetic reconnaissance of the Cook Inlet area, Alaska: U.S. Geological Survey Open-File Report 60-59, Report: 58 p.; 9 Plates: 27.85 x 35.82 inches or smaller, https://doi.org/10.3133/ofr6059.","productDescription":"Report: 58 p.; 9 Plates: 27.85 x 35.82 inches or smaller","costCenters":[],"links":[{"id":421784,"rank":11,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421783,"rank":10,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-3explanation.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421782,"rank":9,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421781,"rank":8,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421780,"rank":7,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421779,"rank":6,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-6.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421778,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421777,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421776,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1960/0059/figure-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":421775,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0059/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":144657,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0059/report-thumb.jpg"}],"scale":"500000","country":"United States","state":"Alaska","otherGeospatial":"Cook Inlet area","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -154.86692834754194,\n 58.461367338468136\n ],\n [\n -148.58541629436866,\n 58.461367338468136\n ],\n [\n -148.58541629436866,\n 61.78410578839723\n ],\n [\n -154.86692834754194,\n 61.78410578839723\n ],\n [\n -154.86692834754194,\n 58.461367338468136\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685c25","contributors":{"authors":[{"text":"Grantz, Arthur agrantz@usgs.gov","contributorId":2585,"corporation":false,"usgs":true,"family":"Grantz","given":"Arthur","email":"agrantz@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":168548,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zietz, Isidore","contributorId":76708,"corporation":false,"usgs":true,"family":"Zietz","given":"Isidore","affiliations":[],"preferred":false,"id":168549,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Andreasen, Gordon E.","contributorId":94272,"corporation":false,"usgs":true,"family":"Andreasen","given":"Gordon E.","affiliations":[],"preferred":false,"id":168550,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":2958,"text":"wsp1624 - 1960 - Surface water supply of the United States, 1959, Part 2-B, South Atlantic slope and eastern Gulf of Mexico Basins, Ogeechee River to Pearl River","interactions":[],"lastModifiedDate":"2012-02-02T00:05:35","indexId":"wsp1624","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"1624","title":"Surface water supply of the United States, 1959, Part 2-B, South Atlantic slope and eastern Gulf of Mexico Basins, Ogeechee River to Pearl River","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1624","usgsCitation":"Wells, J.V., 1960, Surface water supply of the United States, 1959, Part 2-B, South Atlantic slope and eastern Gulf of Mexico Basins, Ogeechee River to Pearl River: U.S. Geological Survey Water Supply Paper 1624, x, 488 p. :ill., tables ;25 cm., https://doi.org/10.3133/wsp1624.","productDescription":"x, 488 p. :ill., tables ;25 cm.","costCenters":[],"links":[{"id":138970,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1624/report-thumb.jpg"},{"id":29667,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1624/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af8e4b07f02db6943a2","contributors":{"authors":[{"text":"Wells, J. V. B.","contributorId":57037,"corporation":false,"usgs":true,"family":"Wells","given":"J.","email":"","middleInitial":"V. B.","affiliations":[],"preferred":false,"id":146044,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":16547,"text":"ofr60155 - 1960 - Geology of the Jackson Mountains, Humbolt County, Nevada","interactions":[{"subject":{"id":16547,"text":"ofr60155 - 1960 - Geology of the Jackson Mountains, Humbolt County, Nevada","indexId":"ofr60155","publicationYear":"1960","noYear":false,"title":"Geology of the Jackson Mountains, Humbolt County, Nevada"},"predicate":"SUPERSEDED_BY","object":{"id":36247,"text":"b1141D - 1963 - General geology of the Jackson Mountains, Humboldt County, Nevada","indexId":"b1141D","publicationYear":"1963","noYear":false,"chapter":"D","title":"General geology of the Jackson Mountains, Humboldt County, Nevada"},"id":1}],"supersededBy":{"id":36247,"text":"b1141D - 1963 - General geology of the Jackson Mountains, Humboldt County, Nevada","indexId":"b1141D","publicationYear":"1963","noYear":false,"title":"General geology of the Jackson Mountains, Humboldt County, Nevada"},"lastModifiedDate":"2018-12-19T08:34:12","indexId":"ofr60155","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-155","title":"Geology of the Jackson Mountains, Humbolt County, Nevada","docAbstract":"The Jackson Mountains, a prominent range near the center of Humboldt County, Nevada, are of interest because the Cretaceous rocks in the range record the effects of a late Cretaceous to early Tertiary orogeny. Such an orogeny has been assumed to have effected all of the Great Basin, but the rock record is sufficiently complete to provide positive dating in only a few areas such as the Jackson Mountains.
The oldest rocks in the range are the Permian and older(?) volcanic rocks of the Happy Creek volcanic series which make up most of the northern half of the range. In a few places the Happy Creek volcanic series grades upward into undivided Permian and Triassic rocks, which consist of interbedded elastic sedimentary rocks and basic volcanic rocks, with some shaly and siliceous limestone. The Happy Creek volcanic series is also overlain by an unnamed predominantly limestone unit of Triassic age. A phyllite and slate unit of probable Triassic ass is in fault contact with the Permian and Triassic undivided rocks. At several other localities the Happy Creek volcanic rocks are overlain by the early Cretaceous King Lear formation or by the Cretaceous or Tertiary Pansy Lee conglomerate, which are the two units of chief importance in dating the Cretaceous and early Tertiary orogenic events.
The King Lear formation consists of locally derived pebble and boulder conglomerate and interbedded siltstone and greywacke, and lenses of limestone.
The Pansy Lee conglomerate is a pebble conglomerate with considerable interbedded coarse-grained sandstone. The pebbles consist of chart and quartzite completely unlike rocks pow exposed in the Jackson mountains.
Dioritic rocks were intruded both before and after the King Lear formation was deposited. Granodioritic intrusive bodies in the range cut rocks no younger than Triassic but the granodiorite is believed to be of late Cretaceous or early Tertiary age.
Tertiary intrusive and extrusive volcanic rocks and sedimentary rocks are widely distributed along the east side and south end of the range.
The most extensive tectonic feature of the Jackson Mountains is the Deer Creek thrust, which is discontinuously exposed from Rattlesnake Canyon northeastward to the north side of Deer Creek Peak. The thrust has brought the Happy Creek volcanic series over the King Lear and Pansy Lee formations, and thus it is of late Cretaceous or early Tertiary age.
An earlier period of Cretaceous deformation is shown by a northeastward-plunging syncline in the King Lear formation on the southeast side of King Lear Peak.
Pre-Cretaceous deformation is shown by a tight fold in lime/atom of the undivided Permian and Triassic unit beneath the King Lear formation at the mouth of Rattlesnake Canyon.
The late Tertiary deformation vas almost exclusively a response to vertically directed stresses, which generally produced high angle faults rather than folds. The range has probably been uplifted principally by displacement on faults that are buried beneath the alluvium some distance to the east and vest of the range.
Ore deposits in the range include tome small but high-grade iron deposits, some low-grade quicksilver deposits and some small copper prospects.
The iron occurs in veins that cut the Happy Creek volcanic series or as replacement bodies near the contact between diorite and the Happy Creek volcanics. Bleached volcanic rocks that are cut by numerous closely spaced joints with a film of hematite in the volcanic rock on either aids of the joints suggest that the iron of the iron deposits has been derived from the Happy Creek volcanic rocks. The diorite intrusives may have provided heat and solutions to mobilize the iron of the volcanic rocks.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr60155","usgsCitation":"Willden, C.R., 1960, Geology of the Jackson Mountains, Humbolt County, Nevada: U.S. Geological Survey Open-File Report 60-155, Report: x, 120 p.; 2 Plates: 30.14 x 41.18 inches and 24.00 x 15.74 inches, https://doi.org/10.3133/ofr60155.","productDescription":"Report: x, 120 p.; 2 Plates: 30.14 x 41.18 inches and 24.00 x 15.74 inches","costCenters":[],"links":[{"id":148837,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0155/report-thumb.jpg"},{"id":360543,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0155/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":360542,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0155/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":360544,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0155/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nevada","county":"Humbolt County","otherGeospatial":"Jackson Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.75,\n 41\n ],\n [\n -118.25,\n 41\n ],\n [\n -118.25,\n 41.5\n ],\n [\n -118.75,\n 41.5\n ],\n [\n -118.75,\n 41\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acee4b07f02db67fee1","contributors":{"authors":[{"text":"Willden, Charles Ronald","contributorId":84388,"corporation":false,"usgs":true,"family":"Willden","given":"Charles","email":"","middleInitial":"Ronald","affiliations":[],"preferred":false,"id":173030,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2952,"text":"wsp1554 - 1960 - Surface water supply of the United States, 1958, part 2-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","interactions":[],"lastModifiedDate":"2012-02-02T00:05:33","indexId":"wsp1554","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"1554","title":"Surface water supply of the United States, 1958, part 2-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1554","usgsCitation":"Wells, J.V., 1960, Surface water supply of the United States, 1958, part 2-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River: U.S. Geological Survey Water Supply Paper 1554, x, 443 p. :ill. ;25 cm., https://doi.org/10.3133/wsp1554.","productDescription":"x, 443 p. :ill. ;25 cm.","costCenters":[],"links":[{"id":139150,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1554/report-thumb.jpg"},{"id":29661,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1554/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af8e4b07f02db69448a","contributors":{"authors":[{"text":"Wells, J. V. B.","contributorId":57037,"corporation":false,"usgs":true,"family":"Wells","given":"J.","email":"","middleInitial":"V. B.","affiliations":[],"preferred":false,"id":146038,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":43165,"text":"ofr6030 - 1960 - Gravity maps of the South Standard and Chief Oxide areas, East Tintic district, Utah","interactions":[{"subject":{"id":43165,"text":"ofr6030 - 1960 - Gravity maps of the South Standard and Chief Oxide areas, East Tintic district, Utah","indexId":"ofr6030","publicationYear":"1960","noYear":false,"title":"Gravity maps of the South Standard and Chief Oxide areas, East Tintic district, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":6149,"text":"pp516D - 1967 - Geologic interpretation of gravity and aeromagnetic maps of Tintic Valley and adjacent areas, Tooele and Juab Counties, Utah","indexId":"pp516D","publicationYear":"1967","noYear":false,"chapter":"D","title":"Geologic interpretation of gravity and aeromagnetic maps of Tintic Valley and adjacent areas, Tooele and Juab Counties, Utah"},"id":1}],"supersededBy":{"id":6149,"text":"pp516D - 1967 - Geologic interpretation of gravity and aeromagnetic maps of Tintic Valley and adjacent areas, Tooele and Juab Counties, Utah","indexId":"pp516D","publicationYear":"1967","noYear":false,"title":"Geologic interpretation of gravity and aeromagnetic maps of Tintic Valley and adjacent areas, Tooele and Juab Counties, Utah"},"lastModifiedDate":"2019-06-21T09:31:54","indexId":"ofr6030","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"60-30","title":"Gravity maps of the South Standard and Chief Oxide areas, East Tintic district, Utah","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr6030","usgsCitation":"Cook, K.L., 1960, Gravity maps of the South Standard and Chief Oxide areas, East Tintic district, Utah: U.S. Geological Survey Open-File Report 60-30, 2 Plates: 26.54 x 31.73 inches and 25.11 x 21.05 inches, https://doi.org/10.3133/ofr6030.","productDescription":"2 Plates: 26.54 x 31.73 inches and 25.11 x 21.05 inches","costCenters":[],"links":[{"id":176391,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0030/report-thumb.jpg"},{"id":364877,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0030/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364878,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0030/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","otherGeospatial":"Tintic","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.89163208007812,\n 39.95054298488249\n ],\n [\n -111.8030548095703,\n 39.95054298488249\n ],\n [\n -111.8030548095703,\n 39.97764627359865\n ],\n [\n -111.89163208007812,\n 39.97764627359865\n ],\n [\n -111.89163208007812,\n 39.95054298488249\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db67209d","contributors":{"authors":[{"text":"Cook, Kenneth L.","contributorId":91099,"corporation":false,"usgs":true,"family":"Cook","given":"Kenneth","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":227820,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2915,"text":"wsp1304 - 1960 - Compilation of records of surface waters of the United States through September 1950: Part 2-B. South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","interactions":[],"lastModifiedDate":"2022-01-18T19:18:26.32014","indexId":"wsp1304","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"1304","title":"Compilation of records of surface waters of the United States through September 1950: Part 2-B. South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1304","usgsCitation":"Wells, J.V., 1960, Compilation of records of surface waters of the United States through September 1950: Part 2-B. South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River: U.S. Geological Survey Water Supply Paper 1304, Report: v, 399 p.; 1 Plate: 35.00 × 40.90 inches, https://doi.org/10.3133/wsp1304.","productDescription":"Report: v, 399 p.; 1 Plate: 35.00 × 40.90 inches","costCenters":[],"links":[{"id":394461,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24306.htm"},{"id":29616,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1304/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":29615,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1304/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":139197,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1304/report-thumb.jpg"}],"country":"United States","state":"Alabama, Florida, Georgia, Louisiana, Mississippi. South Carolina","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.333,\n 25\n ],\n [\n -80,\n 25\n ],\n [\n -80,\n 35\n ],\n [\n -90.333,\n 35\n ],\n [\n -90.333,\n 25\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1de4b07f02db6a99d5","contributors":{"authors":[{"text":"Wells, J. V. B.","contributorId":57037,"corporation":false,"usgs":true,"family":"Wells","given":"J.","email":"","middleInitial":"V. B.","affiliations":[],"preferred":false,"id":145999,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1977,"text":"wsp1489 - 1960 - Geology and ground water in the Platte-Republican Rivers watershed and the Little Blue River basin above Angus, Nebraska, with a section on chemical quality of the ground water","interactions":[],"lastModifiedDate":"2023-01-10T21:09:29.909547","indexId":"wsp1489","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","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":"1489","title":"Geology and ground water in the Platte-Republican Rivers watershed and the Little Blue River basin above Angus, Nebraska, with a section on chemical quality of the ground water","docAbstract":"This report describes an area of about 7,300 square miles in south-central Nebraska. Approximately one-fourth of the area, largely at its east end, consists of an undissected southeastward-sloping upland plain and is almost wholly irrigable; the remainder is in various stages of dissection and only parts of it are suitable for irrigation. Although some of the deeper lying bedrock formations are potential sources of water supply, they are not likely to be tapped in the near future because abundant supplies are available at shallower depth from semiconsolidated and unconsolidated deposits. \r\n\r\nThe Ogallala formation of Tertiary (Pliocene) age consists of gravel, sand, silt, and volcanic ash, some layers of which are partly cemented. It was deposited by eastward-flowing streams, which formed a constructional plain above a surface into which the streams had previously eroded broad valleys. In turn, valleys were cut into the surface of the Ogallala before the overlying deposits of gravel, sand, silt, and clay of Quaternary (Pleistocene) age were laid down, also forming a constructional plain. During Recent time, streams have dissected the older deposits and have deposited thin alluvium in their valleys; also, several parts of the area have become mantled by wind-deposited sand. Because during Tertiary and Quaternary time the area repeatedly was the site of deposition and erosion, the thickness of all the stratigraphic units differs markedly from place to place. In general, however, the Ogallala formation thins eastward and in the central and eastern parts of the area is overlain by the eastward-thickening deposits of Pleistocene age. The maximum thickness of the Ogallala formation is about 500 feet, and the maximum thickness of the Pleistocene deposits is a little more than 300 feet. Each thins to a featheredge and is completely absent in parts of the area. \r\n\r\nThe water-bearing part of the combined Tertiary and Pleistocene deposits is considered to be a single zone of saturation because the ground water, as it percolates southeastward beneath the area, moves out of the Tertiary and into the Quaternary deposits without apparent hindrance. The water that enters the area as underflow from the west is augmented within the area by water that infiltrates from the land surface. The principal sources of irrigating water are precipitation, seepage from canals and reservoirs, and applied irrigation water. Except for the water withdrawn through wells or discharged by natural processes where valleys have been cut into the zone of saturation, ground water leaves the area as underflow into the Platte River valley on the north, the Blue River drainage basin on the east, or the Republican River valley on the south. \r\n\r\nPart of the water used for irrigation and watering livestock and all the water used in rural and urban homes, in public buildings, and for industrial purposes is obtained from wells, To date (1952) there is no indication that the supply of ground water is being depleted faster than it is being replenished; instead, studies indicate that greater quantities can be withdrawn without causing an excessive decline of the water table. An increase of ground-water withdrawals to a sustainable maximum, however, will be possible only if the points of withdrawal are scattered fairly uniformly. It is estimated that annual withdrawals per township should not exceed 2,100 acre-feet where infiltrating precipitation is the only source of recharge, or 3,000 acre-feet where other sources of recharge are significant. Although perennial withdrawals of this amount could be sustained indefinitely, they would cause some lowering of the water table and eventually a decrease in the amount of water discharged from the area by natural means. \r\n\r\nThe ground water is of the calcium bicarbonate type. In much of the area it is hard or very hard, and in places it contains excessive amounts of iron. In all other respects the water is chemically suitable for domesti","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1489","usgsCitation":"Johnson, C.R., and Brennan, R., 1960, Geology and ground water in the Platte-Republican Rivers watershed and the Little Blue River basin above Angus, Nebraska, with a section on chemical quality of the ground water: U.S. Geological Survey Water Supply Paper 1489, Report: iv, 142 p.; 4 Plates: 19.00 x 42.46 inches, https://doi.org/10.3133/wsp1489.","productDescription":"Report: iv, 142 p.; 4 Plates: 19.00 x 42.46 inches","costCenters":[],"links":[{"id":27356,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1489/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27354,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1489/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27353,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1489/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":137664,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1489/report-thumb.jpg"},{"id":27357,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1489/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27355,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1489/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nebraska","otherGeospatial":"Little Blue River basin, Platte-Republican Rivers watershed","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -97.95,\n 41.0833\n ],\n [\n -102.0833,\n 41.0833\n ],\n [\n -102.0833,\n 40\n ],\n [\n -97.95,\n 40\n ],\n [\n -97.95,\n 41.0833\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db686027","contributors":{"authors":[{"text":"Johnson, C. R.","contributorId":14378,"corporation":false,"usgs":true,"family":"Johnson","given":"C.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":144466,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brennan, Robert","contributorId":105695,"corporation":false,"usgs":true,"family":"Brennan","given":"Robert","email":"","affiliations":[],"preferred":false,"id":144467,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}