The area of the Piceance Creek basin between the Colorado and White Rivers includes approximately 1,600 square miles and is characterized by an extensive plateau that rises 1,000 to more than 4,000 feet above the surrounding lowlands. Relief is greatest in Naval Oil-Shale Reserves Nos. 1 and 3 near the south margin of the area, where the spectacular Roan Cliffs tower above the valley of the Colorado River.
The oldest rocks exposed in the mapped area are sandstone, shale, and coal beds of the Mesaverde group of Late Cretaceous age, which crop out along the east margin of the area. Overlying the Mesaverde is an unnamed sequence of dark-colored sandstone and shale, Paleocene in age. The Ohio Creek conglomerate, composed of black and red chert and quartzite pebbles in a white sandstone matrix, is probably the basal unit in the Paleocene sequence. The Wasatch formation of early Eocene age overlies the Paleocene sedimentary rocks. It is composed of brightly colored shale, lenticular beds of sandstone, and a few thin beds of fresh-water limestone. The Kasatch formation interfingers with and is overlain by the Green River formation of middle Eocene age.
The Green River formation has been divided into the Douglas Creek, Garden Gulch, Anvil Points, Parachute Creek, and Evacuation Creek members. The basal and uppermost members, the Douglas Creek and Evacuation Creek, respectively, are predominantly sandy units. The two middle members, the Garden Gulch and Parachute Creek, are composed principally of finer clastic rocks. The Anvil Points member is present only on the southeast, east, and northeast margins of the area. It is a nearshore facies composed principally of sandstone and is the equivalent of the Douglas Creek, Garden Gulch, and the lower part of the Parachute Creek members.
All of the richer exposed oil-shale beds are found in the Parachute Creek member, which is divided into two oil-shale zones by a series of low-grade oilshale beds. The upper oil-shale zone has several key beds and zones which can be traced throughout most of the mapped area. One of these, the Mahogany ledge or zone, is a group of very rich oil-shale beds at the base of the upper oil-shale zone. Drilling for oil and gas in the northeastern part of the area has revealed rich oil-shale zones in the Garden Gulch member also.
Local unconformities within and at the base of the Evacuation Creek member are exposed at several places along Piceance Creek and at one place near the mouth of Yellow Creek; otherwise, the rock sequence is conformable.
The mapped area is the major part of a large syncline, modified by numerous smaller structural features. Fractures, probably associated genetically with the minor structural features, are present in the central part of the area. These fractures are high-angle normal faults with small displacement. They occur in pairs with the intervening block downdropped. Two sets of joints are prominent, one trending northwest and the other northeast. The joint systems control the drainage pattern in the south-central part of the area.
More than 20,000 feet of sedimentary rocks underlies the area. Many of the formations yield oil or gas in northwestern Colorado, northeastern Utah, and southwestern Wyoming. The Piceance Creek gas field, in which gas occurs in the Douglas Creek member of the Green River formation, is the largest oil or gas field discovered thus far within the area.
About 7,000 million barrels of oil is contained in oil shale that yields an average of 45 gallons per ton from a continuous sequence 5 or more feet thick in the Mahogany zone. Oil shale in the Mahogany zone and adjacent beds that yields an average of 30 gallons of oil per ton from a continuous sequence 15 or more feet thick contains about 91,000 million barrels of oil. Similar shale in deeper zones in the northern part of the area, for which detailed estimates have not been prepared, are now known to contain at least an additional 72,000 million barrels of oil. Oil shale in a sequence 15 or more feet thick that yields an average of 25 gallons of oil per ton contains about 154,000 million barrels of oil in the Mahogany zone and adjacent beds; such shale in deeper zones in the northern part of the area probably contains at least an additional 157,000 million barrels of oil, although detailed estimates were not made. Oil shale in a sequence greater than 15 feet thick that yields an average of 15 gallons of oil per ton contains more than 900,000 million barrels of oil. These estimates of the oil content of the deposit do not take into account any loss in mining or processing of the shale.
","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/b1082L","usgsCitation":"Donnell, J., 1961, Tertiary geology and oil-shale resources of the Piceance Creek basin between the Colorado and White Rivers, northwestern Colorado: U.S. Geological Survey Bulletin 1082, Report: v, 56 p.; 7 Plates: 33.54 x 39.62 inches or smaller, https://doi.org/10.3133/b1082L.","productDescription":"Report: v, 56 p.; 7 Plates: 33.54 x 39.62 inches or smaller","startPage":"835","endPage":"891","costCenters":[],"links":[{"id":100042,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082l/report.pdf","text":"Report","size":"5.76 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":100043,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-48.pdf","text":"Plate 48","size":"5.31 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 48"},{"id":100044,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-49.pdf","text":"Plate 49","size":"889 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 49"},{"id":100045,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-50.pdf","text":"Plate 50","size":"411 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 50"},{"id":100046,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-51.pdf","text":"Plate 51","size":"308 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 51"},{"id":100047,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-52.pdf","text":"Plate 52","size":"309 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 52"},{"id":100048,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-53.pdf","text":"Plate 53","size":"387 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 53"},{"id":100049,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082l/plate-54.pdf","text":"Plate 54","size":"872 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 54"},{"id":172973,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082l/report-thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Colorado River, Piceance Creek basin, White River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.05303955078125,\n 40.04023218690451\n ],\n [\n -109.04754638671875,\n 39.2832938689385\n ],\n [\n -108.9349365234375,\n 39.24501680713314\n ],\n [\n -108.78662109375,\n 39.16839998800286\n ],\n [\n -108.56414794921875,\n 39.06718050308463\n ],\n [\n -108.44741821289062,\n 39.04585261214505\n ],\n [\n -108.32794189453125,\n 39.10768574604533\n ],\n [\n -108.23181152343749,\n 39.308800296002914\n ],\n [\n -108.09860229492188,\n 39.4054277294279\n ],\n [\n -107.841796875,\n 39.51145753426751\n ],\n [\n -107.72918701171875,\n 39.59722324495565\n ],\n [\n -107.71820068359374,\n 39.71986348549764\n ],\n [\n -107.81158447265624,\n 39.84439484396462\n ],\n [\n -108.0010986328125,\n 39.9434364619742\n ],\n [\n -108.15490722656249,\n 40.052847601823984\n ],\n [\n -108.30047607421876,\n 40.143189742924406\n ],\n [\n -108.42132568359375,\n 40.19670806662855\n ],\n [\n -108.533935546875,\n 40.18307014852534\n ],\n [\n -108.67538452148438,\n 40.163132874122084\n ],\n [\n -108.7591552734375,\n 40.09908414736847\n ],\n [\n -109.05303955078125,\n 40.04023218690451\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db68500d","contributors":{"authors":[{"text":"Donnell, John R.","contributorId":84330,"corporation":false,"usgs":true,"family":"Donnell","given":"John R.","affiliations":[],"preferred":false,"id":235200,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47384,"text":"b1082J - 1961 - Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","interactions":[{"subject":{"id":12663,"text":"ofr5814 - 1956 - Geologic and structure contour maps of the Carlile quadrangle, Crook County, Wyoming","indexId":"ofr5814","publicationYear":"1956","noYear":false,"title":"Geologic and structure contour maps of the Carlile quadrangle, Crook County, Wyoming"},"predicate":"SUPERSEDED_BY","object":{"id":47384,"text":"b1082J - 1961 - Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","indexId":"b1082J","publicationYear":"1961","noYear":false,"chapter":"J","title":"Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming"},"id":1},{"subject":{"id":47384,"text":"b1082J - 1961 - Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","indexId":"b1082J","publicationYear":"1961","noYear":false,"chapter":"J","title":"Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming"},"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":"2017-10-18T15:31:20","indexId":"b1082J","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"J","title":"Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming","docAbstract":"The Carlile quadrangle-is along the northwestern flank of the Black Hills uplift in Crook County, Wyo. The area-is primarily one of canyons and divides that are a result of downcutting by the Belle Fourche River and its tributaries through an alternating succession of sandstone, siltstone, and mudstone or shale beds. The present topography is also influenced by the regional structure, as reflected by the beds that dip gently westward and by the local structural features such as anticlines, domes, synclines, basins, and terraces, which are superimposed upon the regional setting.
Rocks exposed include shale and thin limestone and sandstone beds belonging to the Redwater shale member of the Sundance formation and to the Morrison formation, both of Late Jurassic age; sandstone, siltstone, and mudstone of the Lakota and Fall River formations of Early Cretaceous age; and shale and sandstone of the Skull Creek shale, Newcastle sandstone, and Mowry shale, also of Early Cretaceous age. In the southwestern part of the quadrangle rocks of the Upper Cretaceous series are exposed. These include the Belle Fourche shale, Greenhorn formation, and Carlile shale. Gravel terraces, landslide debris, and stream alluvium comprise the surficial deposits. The Lakota and Fall River formations, which make up the Iriyan Kara group, contain uranium deposits locally in the northern Black Hills. These formations were informally subdivided in order to show clearly the vertical and lateral distribution of the sandstone, siltstone, and mudstone facies within them.
The Lakota was subdivided into a sandstone unit and an overlying mudstone unit; the Fall River was subdivided, in ascending order, into a siltstone unit, a mudstone unit, a sandstone unit, and an upper unit. The lithologic character of the Lakota changes abruptly locally, and the units are quite inconsistent with respect to composition, thickness, and extent. This is in contrast to a notable consistency in the lithologic character and thickness among all the Fall River units, with the exception of the upper unit. Petrographic studies on selected samples of units from both formations show differences in composition between Lakota and Fall River rocks.
The Carlile quadrangle lies immediately east of the monocline that marks the outer limit of the Black Hills uplift, and the rocks in this area have a regional dip of less than 2° outward from the center of the uplift. Superimposed upon the regional uplift are many subordinate structural features anticlines, synclines, domes, basins, and terraces which locally modify the regional features. The most pronounced of these subordinate structural features are the doubly-plunging Pine Ridge, Oil Butte, and Dakota Divide anticlines, and the Eggie Creek syncline. Stress throughout the area was relieved almost entirely through folding; only a few small nearly vertical normal faults were found within the quadrangle.
Uranium has been mined from the Carlile deposit, owned by the Homestake Mining Co. The ore minerals, carnotite and tyuyamnuite occur in a sandstone lens that is enclosed within relatively impermeable clayey beds in the mudstone unit of the Lakota formation. The ore also includes unidentified black vanadium minerals and possibly coffinite. Uranium minerals are more abundant in and adjacent to thicker carbonaceous and silty seams in the sandstone lens. A mixture of fine-grained calcium carbonate and calcium sulfate fills the interstices between detrital quartz grains in mineralized sandstone. Selenium and arsenic are more abundant in samples that are high in uranium.
Drilling on Thorn Divide about 1 mile west of the Carlile mine has roughly outlined concentrations of a sooty black uranium mineral associated with pyrite In two stratigraphic intervals of the Lakota formation. One is in the same sandstone lens that contains the ore at the Carlile mine; the other is in conglomeratic sandstone near the base of the Lakota. These deposits are relatively deep, and no mining has been attempted.
The mineralogy of the Carlile deposits and the lithologic features of the sandstone host rock suggest that uranium and vanadium were transported in the high-valent state by carbonate or sulfate solutions, were extracted from solution by organic material, and were reduced to low-valent states to form an original assemblage of oxides and silicates. These primary minerals were oxidized in place, and the present carnotite-tyuyamunite assemblage was formed. In general, radioactivity analyses correspond fairly closely with chemical analyses of uranium, thus it is believed that only minor solution and migration of uranium has occurred since the present suite of oxidized minerals was formed.
The factors responsible for ore localization are not clear, but probably a combination of three lithologic and structural elements contributed to provide a favorable environment for precipitating uranium from aqueous solutions: abundant carbonaceous material or pyrite in a thin, permeable sandstone enclosed within relatively thick impermeable clays; local structural basins; and a regional structural setting involving a broad syncline between two anticlines. The structural features controlled the regional flow of ground water and the lithologic features controlled the local rate of flow and provided the proper chemical environment for uranium deposition.
Bentonite has been mined from an opencut in the Mowry shale in the southwest part of the quadrangle. A bentonite bed in the Newcastle sandstone also seems to be of minable thickness and quality.
Exploration for petroleum has been unsuccessful within the quadrangle; however, some wells that yielded oil were recently drilled on small anticlines to the west and southeast. It is possible that similar structural features in the Carlile area, that were previously overlooked, may be equally productive.
","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/b1082J","collaboration":"Prepared on behalf of the Atomic Energy Commission and published with permission of the Commission","usgsCitation":"Bergendahl, M., Davis, R.E., and Izett, G., 1961, Geology and mineral deposits of the Carlile quadrangle, Crook County, Wyoming: U.S. Geological Survey Bulletin 1082, Report: v, 93 p.; 5 Plates: 29.49 x 30.66 inches or smaller, https://doi.org/10.3133/b1082J.","productDescription":"Report: v, 93 p.; 5 Plates: 29.49 x 30.66 inches or smaller","startPage":"613","endPage":"706","costCenters":[],"links":[{"id":100028,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-34.pdf","text":"Plate 34","size":"6.32 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 34"},{"id":100029,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-35.pdf","text":"Plate 35","size":"122 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 35"},{"id":100030,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-36.pdf","text":"Plate 36","size":"3.33 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 36"},{"id":100031,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-37.pdf","text":"Plate 37","size":"1.99 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 37"},{"id":100032,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082j/plate-38.pdf","text":"Plate 38","size":"783 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 38"},{"id":172971,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082j/report-thumb.jpg"},{"id":100027,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082j/report.pdf","text":"Report","size":"6.87 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Wyoming","county":"Crook County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -104.89059448242188,\n 44.37295026072434\n ],\n [\n -104.73129272460936,\n 44.37295026072434\n ],\n [\n -104.73129272460936,\n 44.512176171071054\n ],\n [\n -104.89059448242188,\n 44.512176171071054\n ],\n [\n -104.89059448242188,\n 44.37295026072434\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b46b5","contributors":{"authors":[{"text":"Bergendahl, M.H.","contributorId":23538,"corporation":false,"usgs":true,"family":"Bergendahl","given":"M.H.","affiliations":[],"preferred":false,"id":235196,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Davis, R. E.","contributorId":77153,"corporation":false,"usgs":true,"family":"Davis","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":235197,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Izett, G. A.","contributorId":21131,"corporation":false,"usgs":true,"family":"Izett","given":"G. A.","affiliations":[],"preferred":false,"id":235195,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":3523,"text":"cir450 - 1961 - Sonic depth sounder for laboratory and field use","interactions":[],"lastModifiedDate":"2012-02-02T00:05:25","indexId":"cir450","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"450","title":"Sonic depth sounder for laboratory and field use","docAbstract":"The laboratory investigation of roughness in alluvial channels has led to the development of a special electronic device capable of mapping the streambed configuration under dynamic conditions. This electronic device employs an ultrasonic pulse-echo principle, similar to that of a fathometer, that utilizes microsecond techniques to give high accuracy in shallow depths. This instrument is known as the sonic depth sounder and was designed to cover a depth range of 0 to 4 feet with an accuracy of ? 0.5 percent. The sonic depth sounder is capable of operation at frequencies of 500, 1,000 and 2,000 kilocycles. The ultrasonic beam generated at the transducer is designed to give a minimum-diameter interrogating signal over the extended depth range. The information obtained from a sonic depth sounder is recorded on a strip-chart recorder. This permanent record allows an analysis to be made of the streambed configuration under different dynamic conditions. \r\n\r\nThe model 1024 sonic depth sounder was designed principally as a research instrument to meet laboratory needs. As such, it is somewhat limited in its application as a field instrument on large streams and rivers. The principles employed in this instrument, however, have many potentials for field applications such as the indirect measurement of bed load when the bed roughness is ripples and (or) dunes, depth measurement, determination of bed configuration, and determination of depth of scour around bridge piers and abutments. For field application a modification of the present system into a battery-operated lightweight instrument designed to operate at a depth range of 0 to 30 feet is possible and desirable.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir450","usgsCitation":"Richardson, E., Simons, D., and Posakony, G., 1961, Sonic depth sounder for laboratory and field use: U.S. Geological Survey Circular 450, 7 p. :graphs ;27 cm., https://doi.org/10.3133/cir450.","productDescription":"7 p. :graphs ;27 cm.","costCenters":[],"links":[{"id":124420,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1961/0450/report-thumb.jpg"},{"id":30537,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1961/0450/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4b6b","contributors":{"authors":[{"text":"Richardson, E.V.","contributorId":105697,"corporation":false,"usgs":true,"family":"Richardson","given":"E.V.","email":"","affiliations":[],"preferred":false,"id":147088,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Simons, Daryl B.","contributorId":35715,"corporation":false,"usgs":true,"family":"Simons","given":"Daryl B.","affiliations":[],"preferred":false,"id":147087,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Posakony, G.J.","contributorId":13211,"corporation":false,"usgs":true,"family":"Posakony","given":"G.J.","email":"","affiliations":[],"preferred":false,"id":147086,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":13417,"text":"ofr6142 - 1961 - Geology of uranium in the Chadron area, Nebraska and South Dakota","interactions":[],"lastModifiedDate":"2012-02-02T00:06:50","indexId":"ofr6142","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"61-42","title":"Geology of uranium in the Chadron area, Nebraska and South Dakota","docAbstract":"The Chadron area covers 375 square miles about 25 miles southeast of the Black Hills. Recurrent mild tectonic activity and erosion on the Chadron arch, a compound anticlinal uplift of regional extent, exposed 1900 feet of Upper Cretaceous rocks, mostly marine shale containing pyrite and organic matter, and 600 feet of Oligocene and Miocene rocks, mostly terrestrial fine-grained sediment containing volcanic ash. Each Cretaceous formation truncated by the sub-Oligocene unconformity is stained yellow and red, leached, kaolinized, and otherwise altered to depths as great as 55 feet. The composition and profile of the altered material indicate lateritic soil; indirect evidence indicates Eocene(?) age. In a belt through the central part of the area, the Brule formation of Oligocene age is a sequence of bedded gypsum, clay, dolomite, and limestone more than 300 feet thick.\r\n\r\nUranium in Cretaceous shale in 58 samples averages 0.002 percent, ten times the average for the earth\u0019s crust. Association with pyrite and organic matter indicates low valency. The uranium probably is syngenetic or nearly so.\r\n\r\nUranium in Eocene(?) soil in 43 samples averages 0.054 percent, ranging up to 1.12 percent. The upper part of the soil is depleted in uranium; enriched masses in the basal part of the soil consist of remnants of bedrock shale and are restricted to the highest reaches of the ancient oxidation-reduction interface. The uranium is probably in the from of a low-valent mineral, perhaps uraninite. Modern weathering of Cretaceous shale is capable of releasing as much as 0.780 ppm uranium to water. Eocene(?) weathering probably caused enrichment of the ancient soil through 1) leaching of Cretaceous shale, 2) downward migration of uranyl complex ions, and 3) reduction of hydrogen sulfide at the water table.\r\n\r\nUranium minerals occur in the basal 25 feet of the gypsum facies of the Brule formation at the two localities where the gypsum is carbonaceous; 16 samples average 0.066 percent uranium and range up to 0.43 percent. Elsewhere uranium in dolomite and limestone in the basal 25 feet of the gypsum facies in 10 samples averages 0.007 percent, ranging up to 0.12 percent. Localization of the uranium at the base of the gypsum facies suggests downward moving waters; indirect evidence that the water from which the gypsum was deposited was highly alkaline suggests that the uranium was leached from volcanic ash in Oligocene time.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6142","usgsCitation":"Dunham, R.J., 1961, Geology of uranium in the Chadron area, Nebraska and South Dakota: U.S. Geological Survey Open-File Report 61-42, viii, 243 p. :ill., maps ;29 cm., https://doi.org/10.3133/ofr6142.","productDescription":"viii, 243 p. :ill., maps ;29 cm.","costCenters":[],"links":[{"id":146083,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1961/0042/report-thumb.jpg"},{"id":41852,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1961/0042/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":41853,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1961/0042/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c700","contributors":{"authors":[{"text":"Dunham, Robert Jacob","contributorId":74387,"corporation":false,"usgs":true,"family":"Dunham","given":"Robert","email":"","middleInitial":"Jacob","affiliations":[],"preferred":false,"id":167777,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1705,"text":"wsp1475F - 1961 - Ground Water at Grant Village Site, Yellowstone National Park, Wyoming","interactions":[],"lastModifiedDate":"2012-02-10T00:10:06","indexId":"wsp1475F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"1475","chapter":"F","title":"Ground Water at Grant Village Site, Yellowstone National Park, Wyoming","docAbstract":"On behalf of the National Park Service, the U.S. Geological Survey during the summer of 1959 made a study of ground-water conditions in the area of the Grant Village site, along the shore of the West Thumb of Yellowstone Lake, 1 to 2 miles south of the present facilities at West Thumb. The water supply for the present development at West Thumb is obtained from Duck Lake, but the quantity of water available from this source probably will be inadequate for the planned development at Grant Village.\r\n\r\nDuring the investigation, 11 auger holes were bored and 6 test wells were drilled. Aquifer tests by pumping and bailing methods were made at two of the test wells. All material penetrated in the auger holes and test wells is of Quaternary age except the welded tuff of possible Pliocene age that was penetrated in the lower part of test well 4.\r\n\r\nSmall to moderate quantities of water were obtained from the test wells in the area. Test well 2 yielded 35 gpm (gallons per minute) at a temperature of nearly 100 deg F. Test well 6 yielded about 15 gpm at a temperature of 48 deg F. The yield of this well might be increased by perforation of additional sections of casing, followed by further development of the well. Water from the other four test wells was of inadequate quantity, too highly mineralized, or too warm to be effectively utilized.\r\n\r\nMost of the ground water sampled had high concentrations of silica and iron, and part of the water was excessively high in fluoride content. Otherwise, the ground water was of generally suitable quality for most uses.\r\n\r\nThe most favorable area for obtaining water supplies from wells is near the lakeshore, where a large part of the water pumped would be ground-water flow diverted from its normal discharge into the lake. Moderate quantities of relatively cool water of fairly good quality may be available near the lakeshore between test wells 5 and 6 and immediately east of test well 6.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Hydrology of the Public Domain","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1475F","collaboration":"Prepared in cooperation with the National Park Service","usgsCitation":"Gordon, E.D., McCullough, R.A., and Weeks, E.P., 1961, Ground Water at Grant Village Site, Yellowstone National Park, Wyoming: U.S. Geological Survey Water Supply Paper 1475, 173-200 p., https://doi.org/10.3133/wsp1475F.","productDescription":"173-200 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":12519,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://www.nps.gov/history/history/online_books/geology/publications/wsp/1475-F/","linkFileType":{"id":5,"text":"html"}},{"id":137092,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1475f/report-thumb.jpg"},{"id":26783,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1475f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -110.66666666666667,44.25 ], [ -110.66666666666667,44.5 ], [ -110.33333333333333,44.5 ], [ -110.33333333333333,44.25 ], [ -110.66666666666667,44.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671f58","contributors":{"authors":[{"text":"Gordon, Ellis D.","contributorId":12451,"corporation":false,"usgs":true,"family":"Gordon","given":"Ellis","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":143995,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McCullough, Richard A.","contributorId":78712,"corporation":false,"usgs":true,"family":"McCullough","given":"Richard","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":143996,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Weeks, Edwin P. epweeks@usgs.gov","contributorId":2576,"corporation":false,"usgs":true,"family":"Weeks","given":"Edwin","email":"epweeks@usgs.gov","middleInitial":"P.","affiliations":[],"preferred":true,"id":143994,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":1165,"text":"wsp1593 - 1961 - Simplified methods for computing total sediment discharge with the modified Einstein procedure","interactions":[{"subject":{"id":55755,"text":"ofr5721 - 1957 - Simplified methods for computing total sediment discharge with the modified Einstein procedure","indexId":"ofr5721","publicationYear":"1957","noYear":false,"title":"Simplified methods for computing total sediment discharge with the modified Einstein procedure"},"predicate":"SUPERSEDED_BY","object":{"id":1165,"text":"wsp1593 - 1961 - Simplified methods for computing total sediment discharge with the modified Einstein procedure","indexId":"wsp1593","publicationYear":"1961","noYear":false,"title":"Simplified methods for computing total sediment discharge with the modified Einstein procedure"},"id":1}],"lastModifiedDate":"2012-02-02T00:05:16","indexId":"wsp1593","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","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":"1593","title":"Simplified methods for computing total sediment discharge with the modified Einstein procedure","docAbstract":"A procedure was presented in 1950 by H. A. Einstein for computing the total discharge of sediment particles of sizes that are in appreciable quantities in the stream bed. This procedure was modified by the U.S. Geological Survey and adapted to computing the total sediment discharge of a stream on the basis of samples of bed sediment, depth-integrated samples of suspended sediment, streamflow measurements, and water temperature. This paper gives simplified methods for computing total sediment discharge by the modified Einstein procedure. Each of four homographs appreciably simplifies a major step in the computations. Within the stated limitations, use of the homographs introduces much less error than is present in either the basic data or the theories on which the computations of total sediment discharge are based. The results are nearly as accurate mathematically as those that could be obtained from the longer and more complex arithmetic and algebraic computations of the Einstein procedure.","language":"ENGLISH","publisher":"U.S. G.P.O.,","doi":"10.3133/wsp1593","usgsCitation":"Colby, B.R., and Hubbell, D.W., 1961, Simplified methods for computing total sediment discharge with the modified Einstein procedure: U.S. Geological Survey Water Supply Paper 1593, vi, 17 p. ;24 cm., https://doi.org/10.3133/wsp1593.","productDescription":"vi, 17 p. ;24 cm.","costCenters":[],"links":[{"id":137129,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1593/report-thumb.jpg"},{"id":26000,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1593/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264358,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-1.pdf","size":"3161","linkFileType":{"id":1,"text":"pdf"}},{"id":264359,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-2.pdf","size":"2582","linkFileType":{"id":1,"text":"pdf"}},{"id":264360,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-3.pdf","size":"1606","linkFileType":{"id":1,"text":"pdf"}},{"id":264361,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-4.pdf","size":"355","linkFileType":{"id":1,"text":"pdf"}},{"id":264362,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-5.pdf","size":"1808","linkFileType":{"id":1,"text":"pdf"}},{"id":264363,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-6.pdf","size":"1599","linkFileType":{"id":1,"text":"pdf"}},{"id":264364,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-7.pdf","size":"4402","linkFileType":{"id":1,"text":"pdf"}},{"id":264365,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1593/plate-8.pdf","size":"4532","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f9e4b07f02db5f38d7","contributors":{"authors":[{"text":"Colby, Bruce R.","contributorId":59775,"corporation":false,"usgs":true,"family":"Colby","given":"Bruce","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143287,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hubbell, David Wellington","contributorId":88330,"corporation":false,"usgs":true,"family":"Hubbell","given":"David","email":"","middleInitial":"Wellington","affiliations":[],"preferred":false,"id":143288,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":70207362,"text":"70207362 - 1961 - Recent chemical analyses of waters from several closed-basin lakes and their tributaries in the western United States","interactions":[],"lastModifiedDate":"2019-12-18T11:09:00","indexId":"70207362","displayToPublicDate":"1961-12-31T11:04:45","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":"Recent chemical analyses of waters from several closed-basin lakes and their tributaries in the western United States","docAbstract":"Some of the classic closed-basin lakes of the western United States have been resampled, and the waters have been analyzed by modern wet-chemical methods. Included are waters from Borax and Little Borax lakes and Mono Lake in California; Big Soda, Pyramid, and Walker Lakes in Nevada; Abert Lake, Oregon; and Great Salt Lake, Utah. Tributary streams and springs have also been sampled and are reported upon. © 1961, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1421:RCAOWF]2.0.CO;2","issn":"00167606","usgsCitation":"Whitehead, H., and Feth, J.H., 1961, Recent chemical analyses of waters from several closed-basin lakes and their tributaries in the western United States: Geological Society of America Bulletin, v. 72, no. 9, p. 1421-1425, https://doi.org/10.1130/0016-7606(1961)72[1421:RCAOWF]2.0.CO;2.","productDescription":"5 p. ","startPage":"1421","endPage":"1425","costCenters":[],"links":[{"id":370401,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"72","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Whitehead, H.C.","contributorId":50134,"corporation":false,"usgs":true,"family":"Whitehead","given":"H.C.","email":"","affiliations":[],"preferred":false,"id":777818,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Feth, J. H.","contributorId":50495,"corporation":false,"usgs":true,"family":"Feth","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":777819,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220626,"text":"70220626 - 1961 - Subaerially carved Arctic seavalley under a modern epicontinental sea","interactions":[],"lastModifiedDate":"2021-05-21T16:05:08.216125","indexId":"70220626","displayToPublicDate":"1961-12-31T10:54:49","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":"Subaerially carved Arctic seavalley under a modern epicontinental sea","docAbstract":"A shallow seavalley, averaging 6 feet in relief, extends from the mouth of Ogotoruk Creek, northwest Alaska, for 15 miles across the floor of the Chukchi Sea to a depth of 135 feet. The seavalley is considered to be a drowned subaerial valley of Pleistocene age, which was excavated on an eustatically emerged epicontinental shelf during periods of glacially depressed sea level.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1433:SCASUA]2.0.CO;2","usgsCitation":"Scholl, D., and Sainsbury, C., 1961, Subaerially carved Arctic seavalley under a modern epicontinental sea: Bulletin of the Geological Society of America, v. 72, no. 9, p. 1433-1436, https://doi.org/10.1130/0016-7606(1961)72[1433:SCASUA]2.0.CO;2.","productDescription":"4 p.","startPage":"1433","endPage":"1436","costCenters":[],"links":[{"id":385846,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"72","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Scholl, David 0000-0001-6500-6962","orcid":"https://orcid.org/0000-0001-6500-6962","contributorId":204785,"corporation":false,"usgs":true,"family":"Scholl","given":"David","affiliations":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true},{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":816252,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sainsbury, C.L.","contributorId":99968,"corporation":false,"usgs":true,"family":"Sainsbury","given":"C.L.","email":"","affiliations":[],"preferred":false,"id":816253,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220603,"text":"70220603 - 1961 - Some aspects of the geochemistry of sphalerite, Central City District, Colorado","interactions":[],"lastModifiedDate":"2021-05-20T21:57:32.680452","indexId":"70220603","displayToPublicDate":"1961-11-01T16:52:53","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":"Some aspects of the geochemistry of sphalerite, Central City District, Colorado","docAbstract":"Detailed studies of sphalerite, as a part of a larger study of the Central City district, Colorado, have been undertaken to learn something of the physico-chemical environment of ore deposition. More than 90 samples have been analyzed by chemical and spectrochemical methods and these data are interpreted in the light of experimental information.Sphalerite is a widespread and moderately abundant constituent of the gold- and silver-rich veins of the district. It was deposited during one stage of mineralization, in all environments of the concentrically zoned district except in the core. On a district-wide basis it occurs in three mineral assemblages: sphalerite-pyrite- chalcopyrite-tennantite-galena, sphalerite-pyrite-tennantite-galena, and sphalerite-pyrite-enargite-tennan-tite-galena. Quartz and, locally, other gangues are present.The sphalerite samples contain from 12 to 0.05 weight percent iron and detectable amounts of a restricted suite of minor elements, principally manganese, cadmium, copper, and lead. Manganese correlates directly with iron content, but the other minor elements have random correlations.The iron content of Central City sphalerite is interpreted to be mainly a function of activity of sulfur and temperature. Total pressure and minor elements that may enter the structure of either sphalerite or coexisting pyrite are thought to have negligible effects on the amount of iron in the sphalerite.The iron content of the sphalerite and fluid inclusion studies indicate that mineralization occurred over a temperature range from at least 620° C to about 150° C. In general, the temperatures tended to decrease from the vicinity of the central zone outward toward the peripheral zone. The thermal pattern, however, was complex, and marked by local irregularities.The activity of sulfur decreased with temperature, but to an extent such that more sulfur-rich mineral assemblages could form toward the margins of the district.The minor-element content of the sphalerite is governed by the activities of the various components and by the ability of the host mineral to accomodate it. Manganese varies widely because (1) it is geochemically much more abundant than is zinc and (2) it can also enter other minerals on a large scale. Conversely, because the amount of cadmium is small relative to that of zinc and because it enters only sphalerite in quantitatively significant amounts in hydrothermal environments, the cadmium content of sphalerite is constant. The copper content of the sphalerites is low and in good agreement with recent experimental data of Priestley Toulmin 3d.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.56.7.1211","usgsCitation":"Sims, P., and Barton, P.B., 1961, Some aspects of the geochemistry of sphalerite, Central City District, Colorado: Economic Geology, v. 56, no. 7, p. 1211-1237, https://doi.org/10.2113/gsecongeo.56.7.1211.","productDescription":"27 p.","startPage":"1211","endPage":"1237","costCenters":[],"links":[{"id":385819,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Central City","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.53501129150389,\n 39.7789912112384\n ],\n [\n -105.48419952392578,\n 39.7789912112384\n ],\n [\n -105.48419952392578,\n 39.81354685177315\n ],\n [\n -105.53501129150389,\n 39.81354685177315\n ],\n [\n -105.53501129150389,\n 39.7789912112384\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"56","issue":"7","noUsgsAuthors":false,"publicationDate":"1961-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Sims, P.K.","contributorId":78702,"corporation":false,"usgs":true,"family":"Sims","given":"P.K.","affiliations":[],"preferred":false,"id":816130,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barton, P. B. Jr.","contributorId":23683,"corporation":false,"usgs":true,"family":"Barton","given":"P.","suffix":"Jr.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":816131,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70213478,"text":"70213478 - 1961 - Palæomagnetic evidence relevant to a change in the Earth's radius","interactions":[],"lastModifiedDate":"2020-09-18T20:33:47.610301","indexId":"70213478","displayToPublicDate":"1961-04-01T15:12:15","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Palæomagnetic evidence relevant to a change in the Earth's radius","docAbstract":"IT is important to note that if, during an expansion of the Earth, each point on the surface were to move radially outward, then all sampling areas would have the same relative geographical co-ordinates before and after expansion. Palæomagnetic results could not be used to detect an expansion of this type. However, an alternative model of expansion is that in which most or all of the increase in area is reflected by an increase in the area of the ocean basins. We considered Prof. Carey's model of Earth expansion to be of this general type, since he concludes1 that the Atlantic, Indian and Pacific Ocean basins formed by dilatation attendant on expansion. If the ocean basins formed in this way, the method we used would show an increase in the Earth's radius, even if the continents had also grown a lesser amount.
","language":"English","publisher":"Nature Publications","doi":"10.1038/190036b0","usgsCitation":"Cox, A., and Doell, R., 1961, Palæomagnetic evidence relevant to a change in the Earth's radius: Nature, v. 190, p. 36-37, https://doi.org/10.1038/190036b0.","productDescription":"2 p.","startPage":"36","endPage":"37","costCenters":[],"links":[{"id":378543,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"190","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Cox, Allan","contributorId":89949,"corporation":false,"usgs":true,"family":"Cox","given":"Allan","email":"","affiliations":[],"preferred":false,"id":799128,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Doell, Richard R.","contributorId":66683,"corporation":false,"usgs":true,"family":"Doell","given":"Richard R.","affiliations":[],"preferred":false,"id":799129,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1013666,"text":"1013666 - 1961 - Modification of the microhematocrit technique with trout blood","interactions":[],"lastModifiedDate":"2026-04-15T16:13:17.175262","indexId":"1013666","displayToPublicDate":"1961-04-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3624,"text":"Transactions of the American Fisheries Society","active":true,"publicationSubtype":{"id":10}},"title":"Modification of the microhematocrit technique with trout blood","docAbstract":"Commercial and laboratory‐prepared capillary tubes for hematocrit were tested. A 10 percent solution of heparin was found to be best for the preparation of treated capillary tubes. For examination of trout blood laboratory‐prepared capillary tubes were found to be superior to commercial tubes which are designed for human blood. Sharp, pointed heparinized capillary tubes were used with good results for collecting blood from the heart without killing the examined fish. Hematocrits determined directly in such tubes were found to have the same value as those prepared in other ways.
","language":"English","publisher":"American Fisheries Society","doi":"10.1577/1548-8659(1961)90[139:MOTMTW]2.0.CO;2","usgsCitation":"Larsen, H., and Snieszko, S.F., 1961, Modification of the microhematocrit technique with trout blood: Transactions of the American Fisheries Society, v. 90, no. 2, p. 139-142, https://doi.org/10.1577/1548-8659(1961)90[139:MOTMTW]2.0.CO;2.","productDescription":"4 p.","startPage":"139","endPage":"142","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"links":[{"id":131443,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"90","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4fe4b07f02db62851d","contributors":{"authors":[{"text":"Larsen, H.N.","contributorId":101601,"corporation":false,"usgs":true,"family":"Larsen","given":"H.N.","email":"","affiliations":[],"preferred":false,"id":319000,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Snieszko, S. F.","contributorId":13169,"corporation":false,"usgs":true,"family":"Snieszko","given":"S.","middleInitial":"F.","affiliations":[],"preferred":false,"id":318999,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70220623,"text":"70220623 - 1961 - Sulfide ores formed from sulfide-deficient solutions 1","interactions":[],"lastModifiedDate":"2021-05-21T15:25:56.952545","indexId":"70220623","displayToPublicDate":"1961-01-01T10:23:16","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":"Sulfide ores formed from sulfide-deficient solutions 1","docAbstract":"Assuming that many hydrothermal ore deposits are formed from emanations given off from a magma at depth while it cools through the interval in which latent heat of crystallization is generated, it is shown that this cooling interval for magmatic bodies of moderate size must be measured in tens or hundreds of thousands of years. Emanations from such a magma should change at the source with time: relatively insoluble volatiles should depart early and the more soluble ones late; the general order is probably sulfur gases and oxides of carbon, water, chlorides, and fluorides. Experimental and field evidence indicates that this order approximates the increasing solubility of these gases in natural magmas. Theoretical considerations show that within a hydrothermal conduit a relatively small gradient would soon be established between the magma and the surface. A small gradient suggests that temperature drop is a minor factor in precipitating substances in solution, whereas a drop in pressure and reaction with wall rocks or with material precipitated from earlier emanations would be of major importance. The sulfur-rich early emanations tend to react with indigenous iron of the country rock, or with iron carried by carbon dioxide-rich solutions to where a marked pressure drop occurs; either of these reactions will form abundant early iron sulfide. Later sulfur-deficient emanations, which then carry soluble halides of ore metals, react with this early iron sulfide to precipitate the ore mineral sulfides by replacement and deposition with loss of iron to the solution. Precipitation of much sulfide ore is thus commonly accomplished by sulfur that was fixed near the site of the ore body by earlier emanations from the magmatic source; a large amount of ore, however, may be precipitated from late-stage magmatic solutions where they mingle with early-stage sulfur-bearing solutions from a different magmatic source.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.56.1.68","usgsCitation":"Lovering, T.S., 1961, Sulfide ores formed from sulfide-deficient solutions 1: Economic Geology, v. 56, no. 1, p. 68-99, https://doi.org/10.2113/gsecongeo.56.1.68.","productDescription":"32 p.","startPage":"68","endPage":"99","costCenters":[],"links":[{"id":385840,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"56","issue":"1","noUsgsAuthors":false,"publicationDate":"1961-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Lovering, T. S.","contributorId":108085,"corporation":false,"usgs":true,"family":"Lovering","given":"T.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":816247,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220622,"text":"70220622 - 1961 - Sulfide ores formed from sulfide-deficient solutions 1","interactions":[],"lastModifiedDate":"2021-05-21T15:27:07.396307","indexId":"70220622","displayToPublicDate":"1961-01-01T10:23:16","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":"Sulfide ores formed from sulfide-deficient solutions 1","docAbstract":"Assuming that many hydrothermal ore deposits are formed from emanations given off from a magma at depth while it cools through the interval in which latent heat of crystallization is generated, it is shown that this cooling interval for magmatic bodies of moderate size must be measured in tens or hundreds of thousands of years. Emanations from such a magma should change at the source with time: relatively insoluble volatiles should depart early and the more soluble ones late; the general order is probably sulfur gases and oxides of carbon, water, chlorides, and fluorides. Experimental and field evidence indicates that this order approximates the increasing solubility of these gases in natural magmas. Theoretical considerations show that within a hydrothermal conduit a relatively small gradient would soon be established between the magma and the surface. A small gradient suggests that temperature drop is a minor factor in precipitating substances in solution, whereas a drop in pressure and reaction with wall rocks or with material precipitated from earlier emanations would be of major importance. The sulfur-rich early emanations tend to react with indigenous iron of the country rock, or with iron carried by carbon dioxide-rich solutions to where a marked pressure drop occurs; either of these reactions will form abundant early iron sulfide. Later sulfur-deficient emanations, which then carry soluble halides of ore metals, react with this early iron sulfide to precipitate the ore mineral sulfides by replacement and deposition with loss of iron to the solution. Precipitation of much sulfide ore is thus commonly accomplished by sulfur that was fixed near the site of the ore body by earlier emanations from the magmatic source; a large amount of ore, however, may be precipitated from late-stage magmatic solutions where they mingle with early-stage sulfur-bearing solutions from a different magmatic source.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.56.1.68","usgsCitation":"Lovering, T.S., 1961, Sulfide ores formed from sulfide-deficient solutions 1: Economic Geology, v. 56, no. 1, p. 68-99, https://doi.org/10.2113/gsecongeo.56.1.68.","productDescription":"32 p.","startPage":"68","endPage":"99","costCenters":[],"links":[{"id":385841,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"56","issue":"1","noUsgsAuthors":false,"publicationDate":"1961-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Lovering, T. S.","contributorId":108085,"corporation":false,"usgs":true,"family":"Lovering","given":"T.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":816248,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010750,"text":"70010750 - 1961 - Graphic and algebraic solutions of the discordant lead-uranium age problem","interactions":[],"lastModifiedDate":"2020-11-19T17:06:36.661078","indexId":"70010750","displayToPublicDate":"1961-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Graphic and algebraic solutions of the discordant lead-uranium age problem","docAbstract":"Uranium-bearing minerals that give lead-uranium and lead—lead ages that are essentially in agreement, i.e. concordant, generally are considered to have had a relatively simple geologic history and to have been unaltered since their deposition. The concordant ages obtained on such materials are, therefore, assumed to approach closely the actual age of the minerals. Many uranium-bearing samples, particularly uranium ores, give the following discordant age sequences;
The evaluation of discordant lead isotope age data may be separated into two operations. The first operation, with which this paper is concerned, is mechanical in nature and involves the calculation of the different possible concordant ages corresponding to the various processes assumed to have produced the discordant ages. The second operation is more difficult to define and requires, in part, some personal judgement. It includes a synthesis of the possible concordant age solutions with other independent geologic and isotopic evidence. The concordant age ultimately chosen as most acceptable should be consistent not only with the known events in the geologic history of the area, the age relations of the enclosing rocks, and the mineralogic and paragenetic evidence, but also with other independent age measurements and the isotopic data obtained on the lead in related or associated non-radioactive minerals.
The calculation of the possible concordant ages from discordant age data has been greatly simplified by Wetherill's graphical method of plotting the mole ratios of radiogenic
If isotopic data are available for two samples of the same age, x and y, from the same or related deposits or outcrops, graphs of the normalized difference ratios
Practical numerical solutions for many of tho concordant age calculations are not currently available. However, the algebraic equivalents of these new graphical methods give equations which may be programmed for computing machines. For geologically probable parameters the equations of higher order have two positive real roots that rapidly converge on the exact concordant ages corrected for original radiogenic lead and for loss or gain of lead or uranium. Modifications of these general age equations expanded only to the second degree have been derived for use with desk calculators.
These graphical and algebraic methods clearly suggest both the type and minimum number of samples necessary for adequate mathematical analysis of discordant lead isotope age data. This mathematical treatment also makes it clear that discordant lead isotope data alone cannot provide the basis for the choice of one of the possible concordant age solutions. The new equations, in particular, provide an incentive to improve our physical constants, analytical techniques and sampling methods in order that we may derive all of the useful geologic information that is available in a comprehensive lead isotope age study.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(61)90116-8","usgsCitation":"Stieff, L.R., and Stern, T.W., 1961, Graphic and algebraic solutions of the discordant lead-uranium age problem: Geochimica et Cosmochimica Acta, v. 22, no. 2-4, p. 176-199, https://doi.org/10.1016/0016-7037(61)90116-8.","productDescription":"24 p.","startPage":"176","endPage":"199","numberOfPages":"24","costCenters":[],"links":[{"id":219638,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"22","issue":"2-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a29c9e4b0c8380cd5ac33","contributors":{"authors":[{"text":"Stieff, L. R.","contributorId":25619,"corporation":false,"usgs":true,"family":"Stieff","given":"L.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":359564,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Stern, T. W.","contributorId":36122,"corporation":false,"usgs":true,"family":"Stern","given":"T.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":359565,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5230144,"text":"5230144 - 1960 - Bureau of Sport Fisheries and Wildlife Pesticide-Wildlife Review: 1959","interactions":[],"lastModifiedDate":"2012-02-02T00:15:26","indexId":"5230144","displayToPublicDate":"2009-06-09T10:33:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":14,"text":"Circular","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"No. 84 revised","title":"Bureau of Sport Fisheries and Wildlife Pesticide-Wildlife Review: 1959","docAbstract":" Research findings of the Bureau of Sport Fisheries and Wildlife, State agencies and independent research workers in Ala., Ark., Fla., Ga., La., Mass., Mich., Mont., N. Dak., Tex., and Wis. are summarized in this report together with recommendations for reducing damage from pest control operations. Major topics discussed are: Scope of Pesticide-Wildlife Problem; Effects on Wildlife-General; Laboratory Studies and Toxicology; Direct and Indirect Effects of Pesticides on Wildlife; Recent Pesticide Legislation; Value of Wildlife; and Recommendations for Safeguarding Wildlife Values during Pest Control. To avoid undue hazards to wildlife, applications must not exceed the toxicity equivalent of the following concentrations of DDT to the respective forms of wildlife: 0.1 pounds of DDT/acre for crustaceans; 0.2 for fish; 1.0 for amphibians; 2.0 for reptiles and birds; and 5.0 for most mammals. Other suggestions are: 1) Chemical treatment should be used only when entomological research has proved it to be necessary; 2) Before pesticides are used, the effects on different kinds of animals and on animals living in different habitats should be known and carefully considered; 3) Only minimum quantities of chemicals necessary to achieve adequate control of pests should be applied; 4) Pesticides should not be applied to areas that are any larger than is necessary and the chemicals that are used should be the ones whose effects are no more long-lasting than necessary; 5) Whenever possible, chemicals should be applied at the seasons of the year when wildlife damage will be least; 6) Conscientious effort should be made to be sure that pesticides are applied at no more than the intended rates and that no areas receive double doses. Alternates to chemical control are suggested. Among these are biological control, modified agricultural practices, destruction of insect wintering quarters, and the manipulation of water levels. ","language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"DeWitt, J., and George, J., 1960, Bureau of Sport Fisheries and Wildlife Pesticide-Wildlife Review: 1959: Circular No. 84 revised, iv, 36.","productDescription":"iv, 36","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":202937,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":94553,"rank":800,"type":{"id":11,"text":"Document"},"url":"https://hdl.handle.net/2027/mdp.39015051252768?urlappend=%3Bseq=3"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a07e4b07f02db5f995a","contributors":{"authors":[{"text":"DeWitt, J.B.","contributorId":89080,"corporation":false,"usgs":true,"family":"DeWitt","given":"J.B.","email":"","affiliations":[],"preferred":false,"id":343595,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"George, J.L.","contributorId":64749,"corporation":false,"usgs":true,"family":"George","given":"J.L.","email":"","affiliations":[],"preferred":false,"id":343594,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":39053,"text":"pp333 - 1960 - The Foraminiferal Genus Orbitolina in North America","interactions":[],"lastModifiedDate":"2012-02-02T00:09:59","indexId":"pp333","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"333","title":"The Foraminiferal Genus Orbitolina in North America","docAbstract":"The foraminiferal genus Orbitolina has been useful as an index fossil in the Cretaceous rocks of the circumglobal equatorial belt for nearly a century. In Europe and the Near and Middle East enough work has been done on the species to allow their use for approximate correlations within the Cretaceous sedimentary rocks. The study of American specimens of Orbitolina, had been almost neglected although they were used in a rather cursory fashion for markers of the Lower Cretaceous Trinity strata. Three species had been described and assigned to Orbitolina in the United States, but the validity of each of the species had been questioned. A study of the genus Orbitolina, its type species, its morphology and the stratigraphic and geographic distribution in North America are presented in this report.\r\n\r\nStratigraphic sections were measured throughout the area of Lower Cretaceous outcrop in Texas, New Mexico. and Arizona, and samples of Orbitolina were taken from these measured sections. Several thousand thin sections were prepared from which 8 species of Orbitolina, 7 of them new, were recognized. Orbitolina texana (Roemer) was found to be confined to the lower part of the Glen Rose limestone and its equivalents. Orbitolina, minuta n. sp. is essentially confined to the upper part of the Glen Rose limestone and its equivalents. Four of the species are known only from the Arizona and New Mexico region. The species of Orbitolina are useful stratigraphically, but all their characters-internal as well as external-must be considered. The use of thin sections for the study of Orbitolina is essential.\r\n\r\nOne of the first things that had to be determined was the correct concept of the genus Orbitolina. The type species had not been determined by earlier authors, although four species had been suggested at various times. With careful study of the early literature, it became apparent that the type species is Orbitulites lenticulata Lamarck, 1816=Madreporites lenticularis Blumenbach, 1805 by monotypy.\r\n\r\nThe type species had never been studied using modern techniques. This paper presents the first description and illustrations of the type species based on internal as well as external characters. \r\n\r\nThe American forms of Orbitolina had been referred to the species Orbitolina concava (Lamarck) by Silvestri and others. The necessity of understanding O. concava was apparent. Many misconceptions about O. concava had been developed and propagated until the modern concept no longer included the original material on which the svecies was based.\r\n\r\nTopotype material of Orbulites concava Lamarck, 1816, was restudied. For the first time both the internal and the external characters are described and illustrated. Orbitolina concava (Lamarck) is not conspecific with any of the North American forms.\r\n\r\nA thorough knowledge of the morphology of Orbitolina is essential to the interpretation of the features as seen in thin section. Carefully oriented sections were prepared and models built up illustrating the morphology. A new technique was adapted for multiple sectioning of specimens of Orbitolina. Using this technique, several oriented sections can be prepared from one specimen, enabling the correlation of features seen in axial, basal, and tangential sections. This technique should prove useful in the study of similar small objects, and therefore is described and illustrated.\r\n\r\nThe early chambers of microspheric and megalospheric specimens were not well known. A technique for their study was developed and is described. The morphology of the early chambers of both generations is described and illustrated. The nature of the nepionic and neanic chambers of the microspheric generation is described and documented for the first time. The previous supposition of an early trochoid spire in microspheric specimens is rejected in favor of a flaring planispiral coil. This discovery must be considered in a study of the phylogeny.\r\n\r\nCharts are presented showing the strat","language":"ENGLISH","publisher":"Geological Survey (U.S.)","doi":"10.3133/pp333","usgsCitation":"Douglass, R.C., 1960, The Foraminiferal Genus Orbitolina in North America: U.S. Geological Survey Professional Paper 333, iv, 52.; 14 Plates ** Missing pages 48-51 **, https://doi.org/10.3133/pp333.","productDescription":"iv, 52.; 14 Plates ** Missing pages 48-51 **","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":119935,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0333/report-thumb.jpg"},{"id":247707,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0333/plate-15.pdf","size":"1290","linkFileType":{"id":1,"text":"pdf"}},{"id":247708,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0333/plate-16.pdf","size":"1357","linkFileType":{"id":1,"text":"pdf"}},{"id":247709,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0333/plate-17.pdf","size":"1142","linkFileType":{"id":1,"text":"pdf"}},{"id":66282,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0333/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c73d","contributors":{"authors":[{"text":"Douglass, Raymond Charles","contributorId":61029,"corporation":false,"usgs":true,"family":"Douglass","given":"Raymond","email":"","middleInitial":"Charles","affiliations":[],"preferred":false,"id":220865,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":47380,"text":"b1082F - 1960 - Geology and fluorspar deposits, Northgate district, Colorado","interactions":[{"subject":{"id":43620,"text":"ofr5182 - 1951 - Geologic maps of the Northgate fluorspar district, Colorado","indexId":"ofr5182","publicationYear":"1951","noYear":false,"title":"Geologic maps of the Northgate fluorspar district, Colorado"},"predicate":"SUPERSEDED_BY","object":{"id":47380,"text":"b1082F - 1960 - Geology and fluorspar deposits, Northgate district, Colorado","indexId":"b1082F","publicationYear":"1960","noYear":false,"chapter":"F","title":"Geology and fluorspar deposits, Northgate district, Colorado"},"id":1},{"subject":{"id":47380,"text":"b1082F - 1960 - Geology and fluorspar deposits, Northgate district, Colorado","indexId":"b1082F","publicationYear":"1960","noYear":false,"chapter":"F","title":"Geology and fluorspar deposits, Northgate district, 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":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":"2017-10-18T14:10:41","indexId":"b1082F","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":"F","title":"Geology and fluorspar deposits, Northgate district, Colorado","docAbstract":"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":47385,"text":"b1082K - 1960 - Chromite and other mineral deposits in serpentine rocks of the Piedmont Upland, Maryland, Pennsylvania, and Delaware","interactions":[{"subject":{"id":47385,"text":"b1082K - 1960 - Chromite and other mineral deposits in serpentine rocks of the Piedmont Upland, Maryland, Pennsylvania, and Delaware","indexId":"b1082K","publicationYear":"1960","noYear":false,"chapter":"K","title":"Chromite and other mineral deposits in serpentine rocks of the Piedmont Upland, Maryland, Pennsylvania, and Delaware"},"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":"2017-10-18T15:03:08","indexId":"b1082K","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":"K","title":"Chromite and other mineral deposits in serpentine rocks of the Piedmont Upland, Maryland, Pennsylvania, and Delaware","docAbstract":"The Piedmont Upland in Maryland, Pennsylvania, and Delaware is about 160 miles long and at the most 50 miles wide. Rocks that underlie the province are the Baltimore gneiss of Precambrian age and quartzite, gneiss, schist, marble, phyllite, and greenstone, which make up the Glenarm series of early Paleozoic (?) age. These are intruded by granitic, gabbroic, and ultramaflc igneous rocks. Most of the ultramaflc rocks, originally peridotite, pyroxenite, and dunite, have been partly or completely altered to serpentine and talc; they are all designated by the general term serpentine. The bodies of serpentine are commonly elongate and conformable with the enclosing rocks. Many have been extensively quarried for building, decorative, and crushed stone. In addition, chromite, titaniferous magnetite, rutile, talc and soapstone, amphibole asbestos, magnesite, sodium- rich feldspar (commercially known as soda spar), and corundum have been mined or prospected for in the serpentine.
Both high-grade massive chromite and lower grade disseminated chromite occur in very irregular and unpredictable form in the serpentine, and placer deposits of chromite are in and near streams that drain areas underlain by serpentine. A group of unusual minerals, among them kammererite, are typical associates of high-grade massive chromite but are rare in lower grade deposits.
Chromite was first discovered in the United States at Bare Hills, Md., around 1810. Between 1820 and 1850, additional deposits were discovered and mined in Maryland and Pennsylvania, including the largest deposit of massive chromite ever found in the United States the Wood deposit, in the State Line district. A second period of extensive chromite mining came during the late 1860's and early 1870's.
Production figures are incomplete and conflicting. Estimates from the available data indicate that the aggregate production from 27 of 40 known mines before 1900 totaled between 250,000 and 280,000 tons of lode-chromite ore; information is lacking for the other 13. Placer deposits produced considerably more than 15,000 tons of chromite concentrates. Exploratory work in several of the mines and placer deposits during World War I produced about 1,500 long tons of chromite ore, 920 tons of which was sold.
Most of the chromite from Maryland and Pennsylvania was used to manufacture chemical compounds, pigments, and dyes before metallurgical and refractory uses for chromite were developed. Available analyses of the ores indicate that they would satisfy modern requirements for chemical-grade chromite. With the exception of such deposits as the Line Pit and Red Pit mines, the chromite contains too much iron for the best metallurgical grade, but many would be satisfactory low-grade metallurgical chromite. Perhaps 30,000 to 50,000 tons of chromite concentrates that would range from 30 to 54 percent Cr2O3 could be obtained from placer deposits in the State Line and Soldiers Delight districts. A small tonnage of chromite remains in dumps at six of the old mines. Lode and placer deposits in the Philadelphia district, placers in Montgomery County, Md., and possible downward extensions of known ore bodies below the floors of high-grade mines now flooded have not been completely explored. Although other chromite deposits probably lie concealed at relatively shallow depths, no practical method of finding them has been developed.
Small deposits of titaniferous iron ore in serpentine were mined for iron before 1900, but the titanium content troubled furnace operators. Ore bodies are similar in occurrence to chromite deposits; they are massive or disseminated and are found near the edges of serpentine intrusive rocks. The small size of the deposits and comparatively low titanium content limit their importance as a potential source of titanium.
A single rutile deposit in Harford County, Md., has been prospected but not mined. Pockets in schistose chlorite rock, probably altered from pyroxenite, contain as much as 16 percent rutile and average 8 percent. Rutile-bearing rock has been proved to a depth of about 58 feet.
Talc and soapstone deposits that have been worked in the State Line and Jarrettsville-Dublin districts are the result of steatitization of serpentine at its contact with intrusive sodium-rich pegmatites. Deposits in the Marriottsville and Philadelphia districts seem to be related to shear or crush zones in the serpentine, which served as channelways for steatitizing solutions. Massive soapstone was extensively used in the 19th century for furnace, fireplace, and stove linings and for washtubs and bathtubs. Every year from 1906 until 1960 talc and soapstone have been produced from one or more of the deposits in Maryland and Pennsylvania. Deposits near Dublin and Marriottsville, Md., have produced steadily for years and production continues. Lava-grade steatite from Dublin, Md., is manufactured into ceramic products for electrical and refractory purposes.
Slip-fiber amphibole asbestos deposits were known in the area as early as 1837, but early production was limited. The product was used mostly for linings of safes, boiler covers, and paints. During World War I the demand for domestic asbestos for chemical filters led to further development of deposits in Maryland. Between 1916 and 1940 many small veins of good-quality tremolite and anthophyllite were mined, and the fiber was prepared for market at Woodlawn, Md. Only the upper parts of veins, softened by weathering, were usable. Because prospecting was reportedly fairly thorough and known deposits are said to be mined out, and because demand for amphibole asbestos is limited, the possibility of future asbestos production from the area seems small, except as a byproduct of talc quarrying.
Magnesite from several mines in Pennsylvania and Maryland was much in demand between 1828 and 1871 for the manufacture of epsom salt. Exploratory work at the old Goat Hill mines in 1921 indicated that the product could not be profitably prepared for market at that time. Although reportedly high grade, the magnesite veins are thin and small in comparison with other domestic deposits.
Sodium-rich feldspar and corundum deposits occur in pegmatites that are unusual because they characteristically contain little or no quartz and mica and because, insofar as known, they are confined to serpentine rocks. Many of the known deposits of sodium-rich feldspar commercial soda-spar are reportedly mined out. It is possible, however, that other commercial deposits will be found in the area.
At various times from 1825 until about 1892 in Pennsylvania, corundum mined or found at the surface was used to meet a demand of the abrasives industry. The increased use of artificial abrasives has diminished the demand for natural corundum, and interest in the small, irregular Pennsylvania deposits is at present largely historical or mineralogical.
","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/b1082K","usgsCitation":"Pearre, N., and Heyl, A.V., 1960, Chromite and other mineral deposits in serpentine rocks of the Piedmont Upland, Maryland, Pennsylvania, and Delaware: U.S. Geological Survey Bulletin 1082, Report: vii, 126 p.; 8 Plates: 29.51 x 17.78 inches or smaller, https://doi.org/10.3133/b1082K.","productDescription":"Report: vii, 126 p.; 8 Plates: 29.51 x 17.78 inches or smaller","startPage":"707","endPage":"833","costCenters":[],"links":[{"id":172972,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1082k/report-thumb.jpg"},{"id":109308,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20752.htm","linkFileType":{"id":5,"text":"html"},"description":"20752"},{"id":100033,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1082k/report.pdf","text":"Report","size":"9.80 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":100034,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-40.pdf","text":"Plate 40","size":"1.66 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 40"},{"id":100035,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-41.pdf","text":"Plate 41","size":"2.03 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 41"},{"id":100036,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-42.pdf","text":"Plate 42","size":"1.29 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 42"},{"id":100037,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-43.pdf","text":"Plate 43","size":"472 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 43"},{"id":100038,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-44.pdf","text":"Plate 44","size":"325 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 44"},{"id":100039,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-45.pdf","text":"Plate 45","size":"536 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 45"},{"id":100040,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-46.pdf","text":"Plate 46","size":"389 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 46"},{"id":100041,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1082k/plate-47.pdf","text":"Plate 47","size":"640 kB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 47"}],"country":"United States","state":"Delaware, Maryland, Pennsylvania","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -77.45361328125,\n 39.07464374293251\n ],\n [\n -75.0640869140625,\n 39.07464374293251\n ],\n [\n -75.0640869140625,\n 40.51797520038851\n ],\n [\n -77.45361328125,\n 40.51797520038851\n ],\n [\n -77.45361328125,\n 39.07464374293251\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dde4b07f02db5e2512","contributors":{"authors":[{"text":"Pearre, Nancy C.","contributorId":88208,"corporation":false,"usgs":true,"family":"Pearre","given":"Nancy C.","affiliations":[],"preferred":false,"id":235199,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heyl, Allen V. Jr.","contributorId":81168,"corporation":false,"usgs":true,"family":"Heyl","given":"Allen","suffix":"Jr.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":235198,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3194,"text":"wsp1541B - 1960 - Double-mass curves, with a section fitting curves to cyclic data","interactions":[],"lastModifiedDate":"2019-03-27T07:59:56","indexId":"wsp1541B","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":"1541","chapter":"B","title":"Double-mass curves, with a section fitting curves to cyclic data","docAbstract":"The double.-mass curve is used to check the consistency of many kinds of hydrologic data by comparing data for a single station with that of a pattern composed of the data from several other stations in the area The double-mass curve can be used to adjust inconsistent precipitation data. \r\n\r\nThe graph of the cumulative data of one variable versus the cumulative data of a related variable is a straight line so long as the relation between the variables is a fixed ratio. Breaks in the double-mass curve of such variables are caused by changes in the relation between the variables. These changes may be due to changes in the method of data collection or to physical changes that affect the relation. \r\n\r\nApplications of the double-mass curve to precipitation, streamflow, and sediment data, and to precipitation-runoff relations are described. A statistical test for significance of an apparent break in the slope of the double-mass curve is described by an example. Poor correlation between the variables can prevent detection of inconsistencies in a record, but an increase in the length of record tends to offset the effect of poor correlation. \r\n\r\nThe residual-mass curve, which is a modification of the double-mass curve, magnifies imperceptible breaks in the double-mass curve for detailed study. Of the several methods of fitting a smooth curve to cyclic or periodic data, the moving-arc method and the double-integration method deserve greater use in hydrology. Both methods are described in this manual. The moving-arc method has general applicability, and the double integration method is useful in fitting a curve to cycles of sinusoidal form.","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1541B","usgsCitation":"Searcy, J., Hardison, C.H., and Langbein, W., 1960, Double-mass curves, with a section fitting curves to cyclic data: U.S. Geological Survey Water Supply Paper 1541, iv, 36 p., https://doi.org/10.3133/wsp1541B.","productDescription":"iv, 36 p.","startPage":"31","endPage":"66","numberOfPages":"41","costCenters":[],"links":[{"id":138111,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1541b/report-thumb.jpg"},{"id":30179,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1541b/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e47a3e4b07f02db496791","contributors":{"authors":[{"text":"Searcy, James K.","contributorId":44519,"corporation":false,"usgs":true,"family":"Searcy","given":"James K.","affiliations":[],"preferred":false,"id":146412,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hardison, Clayton H.","contributorId":46073,"corporation":false,"usgs":true,"family":"Hardison","given":"Clayton","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":146413,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Langbein, Walter B.","contributorId":98294,"corporation":false,"usgs":true,"family":"Langbein","given":"Walter B.","affiliations":[],"preferred":false,"id":759856,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":3304,"text":"cir422 - 1960 - Availability of ground water at the border stations at Laurier and Ferry, Washington","interactions":[{"subject":{"id":24788,"text":"ofr59137 - 1959 - Availability of ground water at the border stations at Laurier and Ferry, Ferry County, Washington","indexId":"ofr59137","publicationYear":"1959","noYear":false,"title":"Availability of ground water at the border stations at Laurier and Ferry, Ferry County, Washington"},"predicate":"SUPERSEDED_BY","object":{"id":3304,"text":"cir422 - 1960 - Availability of ground water at the border stations at Laurier and Ferry, Washington","indexId":"cir422","publicationYear":"1960","noYear":false,"title":"Availability of ground water at the border stations at Laurier and Ferry, Washington"},"id":1}],"lastModifiedDate":"2024-02-05T22:20:28.092334","indexId":"cir422","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":"422","title":"Availability of ground water at the border stations at Laurier and Ferry, Washington","docAbstract":"In the Laurier area, Washington, the Kettle River has cut into crystalline rocks in the deepest part of the valley. Sand and gravel fill were deposited in the valley during Pleistocene time by melt water from glaciers, and subsequent erosion and alluviation formed three terrace levels. The highest level, on which Laurier Border Station is situated is about 200 feet above present river level The intermediate terrace is 150 to 180 feet above river level. Wells on the intermediate terrace yield about 4 gpm (gallons per minute) per foot of drawdown. Larger yields probably could be obtained from wells on the lowest terrace (flood plain). \r\n\r\nIn the Ferry area the valley fill of the Kettle River valley is as much as 150 feet thick and contains boulders that are as much as 18 inches in diameter. Small to moderate quantities of water probably would be available from wells on the high-terrace level. Large quantities of water are obtained from irrigation wells on the low terrace. The bedrock at both sites is relatively impermeable and probably would yield very meager supplies of water.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir422","usgsCitation":"Walters, K.L., 1960, Availability of ground water at the border stations at Laurier and Ferry, Washington: U.S. Geological Survey Circular 422, iii, 8 p., https://doi.org/10.3133/cir422.","productDescription":"iii, 8 p.","costCenters":[],"links":[{"id":425417,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_53900.htm","text":"Ferry","linkFileType":{"id":5,"text":"html"}},{"id":425416,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_53876.htm","text":"Laurier","linkFileType":{"id":5,"text":"html"}},{"id":30302,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0422/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124408,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0422/report-thumb.jpg"}],"country":"United States","state":"Washington","city":"Ferry, Laurier","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.21290290235422,\n 49\n ],\n [\n -118.54725623478598,\n 49\n ],\n [\n -118.54630574034938,\n 48.955\n ],\n [\n -118.21290290235422,\n 48.9555\n ],\n [\n -118.21290290235422,\n 49\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa9e4b07f02db667ee4","contributors":{"authors":[{"text":"Walters, Kenneth Lyle","contributorId":32493,"corporation":false,"usgs":true,"family":"Walters","given":"Kenneth","email":"","middleInitial":"Lyle","affiliations":[],"preferred":false,"id":146632,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3435,"text":"cir420 - 1960 - Occurrence of strontium in natural water","interactions":[],"lastModifiedDate":"2017-02-21T16:15:35","indexId":"cir420","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":"420","title":"Occurrence of strontium in natural water","docAbstract":"The regions where the stable strontium content of surface waters is relatively low (less than 0.50 ppm) include the Pacific Northwest, Northeastern United States, and the Central Lowlands, Particularly the Lower Mississippi basin and the Western Gulf Coast area. Moderate concentrations of strontium (0.50 to 1.5 ppm) are found in streams of Southeastern United States, most of the Great Plains Region, the Western Mountain and Plateau Regions, and California. Relatively high concentrations of strontium occur in the surface waters of an area that includes Northern and Western Texas and Southern New Mexico and Arizona. Exceptions to the above distribution are due to local geologic conditions.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/cir420","usgsCitation":"Skougstad, M., and Horr, C.A., 1960, Occurrence of strontium in natural water: U.S. Geological Survey Circular 420, iii, 6 p., https://doi.org/10.3133/cir420.","productDescription":"iii, 6 p.","numberOfPages":"11","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":30450,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0420/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":117020,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0420/report-thumb.jpg"}],"country":"United States","publicComments":"Prepared on behalf of the U. S. Atomic Energy Commission and published with the permission of the Commission","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4af4e4b07f02db69219d","contributors":{"authors":[{"text":"Skougstad, M. W.","contributorId":59418,"corporation":false,"usgs":true,"family":"Skougstad","given":"M. W.","affiliations":[],"preferred":false,"id":146907,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Horr, C. Albert","contributorId":43333,"corporation":false,"usgs":true,"family":"Horr","given":"C.","email":"","middleInitial":"Albert","affiliations":[],"preferred":false,"id":146906,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}