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":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":1013666,"text":"1013666 - 1961 - Modification of the microhematocrit technique with trout blood","interactions":[],"lastModifiedDate":"2012-02-02T00:04:21","indexId":"1013666","displayToPublicDate":"1961-01-01T00:00:00","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","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Transactions of the American Fisheries Society","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","collaboration":"103/FH","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.","productDescription":"p. 139-142","startPage":"139","endPage":"142","numberOfPages":"4","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"links":[{"id":131443,"rank":0,"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":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":3783,"text":"cir424 - 1960 - Ground-water supplies in shale and sandstone in Fairfax, Loudoun, and Prince William Counties, Virginia","interactions":[],"lastModifiedDate":"2018-01-02T20:38:28","indexId":"cir424","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":"424","title":"Ground-water supplies in shale and sandstone in Fairfax, Loudoun, and Prince William Counties, Virginia","docAbstract":"The Triassic rocks of northern Virginia may be a potential source of moderately large supplies of ground water for municipal end industrial use if the performance of two deep wells drilled at the site of the new Dulles International Airport is a criterion. These two wells produced 327 and 600 gpm (gallons per minute) from depths of 860-and 955 feet in sedimentary rocks in an immediate area where the previous maximum depth reported was 180 feet and the maximum yield 12 gpm. \r\n\r\nChemical analyses of the water indicates that it is extremely hard--533 and 500 ppm (parts per million) in the two wells--and would require treatment to be satisfactory for domestic and some industrial uses. However, water of better quality may be present at greater depths, and it may be possible to case off the more highly mineralized water. Further exploration and sampling of water from various depths will be necessary for efficient development of the Triassic groundwater reservoir.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir424","usgsCitation":"Johnston, P.M., 1960, Ground-water supplies in shale and sandstone in Fairfax, Loudoun, and Prince William Counties, Virginia: U.S. Geological Survey Circular 424, iv, 7 p. :map, tables. ;27cm., https://doi.org/10.3133/cir424.","productDescription":"iv, 7 p. :map, tables. ;27cm.","costCenters":[],"links":[{"id":30855,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0424/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":117873,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0424/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a96e4b07f02db65a463","contributors":{"authors":[{"text":"Johnston, Paul McKelvey","contributorId":8828,"corporation":false,"usgs":true,"family":"Johnston","given":"Paul","email":"","middleInitial":"McKelvey","affiliations":[],"preferred":false,"id":147591,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":3752,"text":"cir433 - 1960 - Time, distance, and drawdown relationships in a pumped ground-water basin","interactions":[],"lastModifiedDate":"2012-02-02T00:05:38","indexId":"cir433","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":"433","title":"Time, distance, and drawdown relationships in a pumped ground-water basin","docAbstract":"Several reasonable values are assumed for coefficients of transmissibility and storage of lenticular alluvial deposits, These values when substituted in the Theis (1935) nonequilibrium formula as modified by Wenzel (1942) give curves from which time, distance, drawdown relationships are estimated.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir433","usgsCitation":"Kunkel, F., 1960, Time, distance, and drawdown relationships in a pumped ground-water basin: U.S. Geological Survey Circular 433, 8 p. :ill. ;27 cm. + graphs in back pocket., https://doi.org/10.3133/cir433.","productDescription":"8 p. :ill. ;27 cm. + graphs in back pocket.","costCenters":[],"links":[{"id":118313,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0433/report-thumb.jpg"},{"id":30813,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0433/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e47a3e4b07f02db49671f","contributors":{"authors":[{"text":"Kunkel, Fred","contributorId":47766,"corporation":false,"usgs":true,"family":"Kunkel","given":"Fred","email":"","affiliations":[],"preferred":false,"id":147534,"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}]}} ,{"id":52089,"text":"ofr6053 - 1960 - Preliminary report on electromagnetic model studies","interactions":[],"lastModifiedDate":"2012-02-02T00:11:29","indexId":"ofr6053","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"60-53","title":"Preliminary report on electromagnetic model studies","docAbstract":"More than 70 resopnse curves for various models have been obtained using the slingram and turam electromagnetic methods. Results show that for the slingram method, horizontal co-planar coils are usually more sensitive than vertical, co-axial or vertical, co-planar coils. The shape of the anomaly usually is simpler for the vertical coils.","language":"ENGLISH","doi":"10.3133/ofr6053","usgsCitation":"Frischknecht, F., and Mangan, G.B., 1960, Preliminary report on electromagnetic model studies: U.S. Geological Survey Open-File Report 60-53, 12 p.; 80 figs., https://doi.org/10.3133/ofr6053.","productDescription":"12 p.; 80 figs.","costCenters":[],"links":[{"id":178482,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0053/report-thumb.jpg"},{"id":86646,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0053/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48d0e4b07f02db546702","contributors":{"authors":[{"text":"Frischknecht, F.C.","contributorId":63384,"corporation":false,"usgs":true,"family":"Frischknecht","given":"F.C.","email":"","affiliations":[],"preferred":false,"id":244786,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mangan, G. B.","contributorId":86035,"corporation":false,"usgs":true,"family":"Mangan","given":"G.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":244787,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":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":6198,"text":"pp351 - 1960 - Mode of flow of Saskatchewan Glacier, Alberta, Canada","interactions":[],"lastModifiedDate":"2012-02-02T00:06:02","indexId":"pp351","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":"351","title":"Mode of flow of Saskatchewan Glacier, Alberta, Canada","language":"ENGLISH","publisher":"U. S. Govt. Print. Off.,","doi":"10.3133/pp351","usgsCitation":"Meier, M.F., 1960, Mode of flow of Saskatchewan Glacier, Alberta, Canada: U.S. Geological Survey Professional Paper 351, 70 p., https://doi.org/10.3133/pp351.","productDescription":"70 p.","costCenters":[],"links":[{"id":117305,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0351/report-thumb.jpg"},{"id":33359,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0351/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33360,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0351/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33361,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0351/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33362,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0351/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33363,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0351/plate-5.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33364,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0351/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699a6a","contributors":{"authors":[{"text":"Meier, Mark Frederick","contributorId":30982,"corporation":false,"usgs":true,"family":"Meier","given":"Mark","email":"","middleInitial":"Frederick","affiliations":[],"preferred":false,"id":152282,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":15046,"text":"ofr6099 - 1960 - Origin and chemical composition of evaporite deposits","interactions":[],"lastModifiedDate":"2012-02-02T00:07:08","indexId":"ofr6099","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"60-99","title":"Origin and chemical composition of evaporite deposits","docAbstract":"A comparative study of marine evaporite deposits forming at the present time along the pacific coast of central Mexico and evaporite formations of Permian age in West Texas Basin was made in order to determine if the modern sediments provide a basis for understanding environmental conditions that existed during deposition of the older deposits. The field work was supplemented by investigations of artificial evaporite minerals precipitated in the laboratory and by study of the chemical composition of halite rock of different geologic ages.\r\n\r\nThe environment of deposition of contemporaneous marine salt deposits in Mexico is acidic, is strongly reducing a few centimeters below the surface, and teems with microscopic life. Deposition of salt, unlike that of many other sediments, is not wholly a constructional phenomenon. Permanent deposits result only if a favorable balance exists between deposition in the dry season and dissolution in the wet season.\r\n\r\nEvaporite formations chosen for special study in the West Texas Basin are, in ascending order, the Castile, Salado, and Rustler formations, which have a combined thickness of 1200 meters. The Castile formation is largely composed of gypsum rock, the Salado, halite rock, and the Rustler, quartz and carbonate sandstone. The lower part of the Castile formation is bituminous and contains limestone laminae. The Castile and Rustler formations thicken to the south at the expense of salt of the intervening Salado formation.\r\n\r\nThe clastic rocks of the Rustler formation are interpreted as the deposits of a series of barrier islands north of which halite rock of the Salado was deposited. The salt is believed to have formed in shallow water of uniform density that was mixed by the wind. Where water depth exceeded the depth of the wind mixing, density stratification developed, and gypsum was deposited. Dense water of high salinity below the density discontinuity was overlain by less dense, more normally saline water which was derived from the sea to the south. Mixing of the two water layers at their interface diluted the lower layer so as to prevent halite formation, but at the same time the depressed solubility of calcium sulfate in the mixture at the interface caused precipitation of gypsum.\r\n\r\nThe upper water layer is believed to have supported a flourishing microscopic biota whose remains descended into semisterile brine below where reducing conditions prevailed. This environment generated the bituminous gypsum rock. At times, microcrystalline calcium carbonate of probable biochemical origin formed in the upper layer and settled below to form limestone laminae such as those of the lower part of the Castile formation.\r\n\r\nChemical analyses of Permian and present-day salt were compared with analyses of marine salt as old as Cambrian age to determine if evaporite deposits can contribute information on the geologic history of sea water. The results contain uncertainties that cannot be fully resolved, but they suggest that the ratio between ions in sea water has been approximately constant since Precambrian time. In addition, the abrupt initial appearance of rock salt deposits in Cambrian time suggests that the Precambrian ocean may have been rather dilute, but this apparent relationship also could have been caused by other factors.","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr6099","usgsCitation":"Moore, G.W., 1960, Origin and chemical composition of evaporite deposits: U.S. Geological Survey Open-File Report 60-99, 174 p. ill., mpa ;28 cm., https://doi.org/10.3133/ofr6099.","productDescription":"174 p. ill., mpa ;28 cm.","costCenters":[],"links":[{"id":148399,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0099/report-thumb.jpg"},{"id":43958,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0099/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43959,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0099/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":43960,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0099/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66cea1","contributors":{"authors":[{"text":"Moore, George William","contributorId":89123,"corporation":false,"usgs":true,"family":"Moore","given":"George","email":"","middleInitial":"William","affiliations":[],"preferred":false,"id":170474,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"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":52131,"text":"ofr60123 - 1960 - Marine geology and bathymetry of nearshore shelf of Chukchi Sea, Ogotoruk Creek area, northwest Alaska","interactions":[],"lastModifiedDate":"2012-02-02T00:11:28","indexId":"ofr60123","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"60-123","title":"Marine geology and bathymetry of nearshore shelf of Chukchi Sea, Ogotoruk Creek area, northwest Alaska","docAbstract":"During July and August 1958 the U.S. Geological Survey conducted a study in behalf of the Atomic Energy Commission of the oceanography, bathymetry, and marine geology of the nearshore shelf of the Chukchi Sea off the Ogotoruk Creek area, northwest Alaska. Ogotoruk Creek enters the Chukchi Sea about 32 miles southeast of the large cuapate spit of Point Hope at long 165 degrees 44\u001946\u001D W. and lat 68 degrees 05\u001951\u001D N. The Ogotoruk Creek area extends approximately 10 miles west and 7 miles east of the creek mouth. Knowledge of the marine geology and oceanography is confined primarily to the nearshore shelf, which includes about 70 square miles of the shelf and is defined as the sea floor lying shoreward of the 50-foot submarine contour. The 50-foot contour generally lies from 2 to 4 miles from shore. Submarine topography was studied to a distance of 15 miles from shore over an area of approximately 340 square miles.\r\n\r\nA northwest coastal current flows past the Ogotoruk Creek area and during July and August averaged 0.5 mile per hour. Persistent northerly winds cause general upwelling near shore and at times of pronounced upwelling the coastal current was reversed or appreciably reduced in speed. Longshore currents shoreward of the breaker zone averaged 0.3 mile per hour and moved to the east for the greater part of the time of the study.\r\n\r\nThe overall seaward slope of the inner 15 miles of the Chukchi shelf from a depth of 40 to 135 feet is approximately 0 degrees 04\u0019, or about 6 feet per mile. Slopes near shore to depths of 15-20 feet are steep and average 2 degrees 30\u0019. Beyond these depths they increase gradually out to a depth of 40-45 feet. Seaward of this point the shelf is flattest and slopes are as low as 0 degree 01\u0019. This terrace or flat part of the nearshore shelf is about 2 miles wide and descends to a depth of 50-55 feet beyond which the gradient increases to about 0 degree 06\u001D. At depths greater than 85 feet the submarine declivity gradually decreases to 0 degree 03\u0019 at a distance of 15 miles from shore.\r\n\r\nA flat-bottomed trough, Ogotoruk Seavalley, heads about a quarter of a mile from shore off the mouth of Ogotoruk Creek. The shallow seavalley averages only 6 feet in relief and extends 15 miles from shore to a depth of 135 feet. A number of smaller channels also indent the gentle sloping inner Chukchi shelf east of the seavalley and nearshore west of it.\r\n\r\nMany outcrops of Paleozoic and Mesozoic formations on the nearshore shelf indicate that it is a wave-planed platform. Wave planation is thought to have taken place primarily in Sangamon and rpre-Sangamon time (approximately 100,000 to 1,000,000 years ago). Ogotoruk Seavalley is believed to be a drowned subaerial valley which was excavated by Ogotoruk Creek during periods of glacially depressed sea level.\r\n\r\nUnconsolidated sediments overlying the nearshore shelf are chiefly slightly rounded residual gravel which have been derived from submerged outcrops. Detrital sand and silt, contributed from the nearby coastal area during Recent time, overlie the shelf near shore and at depth as much as 50 feet seaward of segments of the coast underlain by fine-grained clastic rocks of Mesozoic age. Owing to a small volume of detrital clasts contributed by the coastal area detrital sedimentation is not prominent over the nearshore shelf.\r\n\r\nBeaches fronting the Ogotoruk Creek area are 30-260 feet wide, range from less than 10 to about 25 feet thick, and are composed of sandy gravel having a median diameter of about 10 mm. Rounded clasts of greywacke, siltstone, limestone, and chert are the principal constituents of the gravel. Longshore currents accompanying moderate storms transport gravel and sand parallel to shore at rates of 5 cubic yards per hour. Sediment transported by longshore currents accumulates as spits at stream mouths and as areas of new beach below rocky headlands.","language":"ENGLISH","doi":"10.3133/ofr60123","usgsCitation":"Scholl, D., and Sainsbury, C., 1960, Marine geology and bathymetry of nearshore shelf of Chukchi Sea, Ogotoruk Creek area, northwest Alaska: U.S. Geological Survey Open-File Report 60-123, 58 p., https://doi.org/10.3133/ofr60123.","productDescription":"58 p.","costCenters":[],"links":[{"id":178881,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0123/report-thumb.jpg"},{"id":86665,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0123/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a1ae4b07f02db606c21","contributors":{"authors":[{"text":"Scholl, D.W.","contributorId":106461,"corporation":false,"usgs":true,"family":"Scholl","given":"D.W.","email":"","affiliations":[],"preferred":false,"id":244851,"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":244850,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"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":57720,"text":"ofr60166 - 1960 - Ground water in Oklahoma","interactions":[],"lastModifiedDate":"2018-11-05T10:34:32","indexId":"ofr60166","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"60-166","title":"Ground water in Oklahoma","docAbstract":"One of the first requisites for the intelligent planning of utilization and control of water and for the administration of laws relating to its use is data on the quantity, quality, and mode of occurrence of the available supplies. The collection, evaluation and interpretation, and publication of such data are among the primary functions of the U. S. Geological Survey, Since 1895 the Congress has made appropriations to the Survey for investigation of the water resources of the Nation. In 1929 the Congress adopted the policy of dollar-for-dollar cooperation with the States and local governmental agencies in water resources investigations of the U. S. Geological Survey, In 1937 a program of ground-water investigations was started in cooperation with the Oklahoma Geological Survey, and in 1949 this program was expanded to include cooperation with the Oklahoma Planning and Resources Board, In 1957 the State Legislature created the Oklahoma Water Resources Board as the principal State water agency and it became the principal local cooperator.
The Mesaverde group of Late Cretaceous age at Sunnyside, Utah consists in ascending order; the Blackhawk formation, Castlegate sandstone and the Price River formation. The Mancos shale inter-tongues with the Blackhawk formation.
The Mancos shale formed in an offshore marine environment, the Blackhawk formation formed in a mixed marine and continental environment and the Castlegate and Price River formations at Sunnyside, Utah formed in a continental environment.
Thin even bedding characterizes the Mancos shale except where it extends as a thin tongue into the Blackhawk formation. Tongues of the Mancos shale in the Blackhawk formation have in places disrupted bedding and locally contain impressions of twigs and branches. Disrupted bedding with mottling, irregular and uneven bedding, and very thick bedding with cross stratification resembling lower foreshore laminae, are primary structures common in modern marine sediments and can also be found in the marine tongues of the Blackhawk formation. Massive, wedge-shaped, cut-and-fill structures characteristic of fluviatile deposits are found in the Castlegate-Price River formations.
Particle size distribution in the marine tongues of the Blackhawk formation shows an increasing coarseness as shoreline deposits are approached. Coal particles are generally absent in the marine sandstones of the Blackhawk formation but are commonly found in abundance in the continental sandstones in the Blackhawk.
The economic coal beds within the Blackhawk formation at Sunnyside have been reported as consisting of a \"Lower\" Sunnyside seam and an \"Upper\" Sunnyside seam. Stratigraphic sections and drill logs indicate that these seams may be splits of one major coal bed and that the term \"Upper\" Sunnyside seam refers to more than one major split.
The relationship of the splits in the Sunnyside coal seams and the lithologic characteristics of the coal indicate that the coal swamp existed on a low-lying coastal plain close to sea level where swamp accumulations were interrupted occasionally by fluviatile deposition.
Subsidence due to compaction of underlying sediments, aggradation as the shoreline regressed as well as slow tectonic subsidence or gradual eustatic rise in sea level are factors which may account for the thickness of the Sunnyside coal beds.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr6018","collaboration":"Prepared in cooperation with the U.S. Bureau of Mines","usgsCitation":"Brodsky, H., 1960, The Mesaverde group at Sunnyside, Utah: U.S. Geological Survey Open-File Report 60-18, Report: 70 p.; 4 Plates: 68.42 x 18.23 inches or smaller, https://doi.org/10.3133/ofr6018.","productDescription":"Report: 70 p.; 4 Plates: 68.42 x 18.23 inches or smaller","costCenters":[],"links":[{"id":489700,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0018/plate-2-3.pdf","text":"Plate 2-3","linkFileType":{"id":1,"text":"pdf"}},{"id":489699,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0018/plate-2-2.pdf","text":"Plate 2-2","linkFileType":{"id":1,"text":"pdf"}},{"id":489698,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1960/0018/plate-2-1.pdf","text":"Plate 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Open-File Report 60-108, 5 p., https://doi.org/10.3133/ofr60108.","productDescription":"5 p.","costCenters":[],"links":[{"id":179249,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a28e4b07f02db610db4","contributors":{"authors":[{"text":"Palmquist, W.N. Jr.","contributorId":76398,"corporation":false,"usgs":true,"family":"Palmquist","given":"W.N.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":244841,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, A.I.","contributorId":82676,"corporation":false,"usgs":true,"family":"Johnson","given":"A.I.","email":"","affiliations":[],"preferred":false,"id":244842,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":3817,"text":"cir434 - 1960 - Progress report on use of water by riparian vegetation, Cottonwood Wash, Arizona","interactions":[],"lastModifiedDate":"2012-02-02T00:05:39","indexId":"cir434","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":"434","title":"Progress report on use of water by riparian vegetation, Cottonwood Wash, Arizona","docAbstract":"Measurements of streamflow, ground-water levels, and meterological data obtained in a 4.1-mile reach of the flood plain of Cottonwood Wash, Mohave County, Ariz., define the use of water by riparian vegetation in that part of the stream valley. The computed evapotranspiration loss during the growing season of 1959 was 175 acre-feet, which represented about 33 percent of the water that entered the reach. The maximum rate of loss during the season was slightly more than 8 acre-feet per week, or about 60 percent of the inflow. \r\n\r\nThe project reach is divided into two parts: An upstream subreach of 2.6 miles and a downstream subreach of 1.5 miles. Seasonal losses in the upstream and downstream subreaches were 75 and 100 acre-feet respectively. Losses in the shorter downstream subreach were larger because of the greater plant population. \r\n\r\nDuring the summer of 1960 the vegetation in the lower subreach will be chemically defoliated as a part of the experiment to determine the savings in water losses that can be effected by modifying riparian vegetation. Tests on chemical defoliants indicate that a single spraying eliminates the leaves on cottonwood trees for 7 or 8 days and that no permanent damage results.","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/cir434","usgsCitation":"Hendricks, E.L., Kam, W., and Bowie, J.E., 1960, Progress report on use of water by riparian vegetation, Cottonwood Wash, Arizona: U.S. Geological Survey Circular 434, iii, 11 p. :ill., map ;27 cm., https://doi.org/10.3133/cir434.","productDescription":"iii, 11 p. :ill., map ;27 cm.","costCenters":[],"links":[{"id":124664,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1960/0434/report-thumb.jpg"},{"id":30887,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1960/0434/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db6493f4","contributors":{"authors":[{"text":"Hendricks, E. L.","contributorId":50126,"corporation":false,"usgs":true,"family":"Hendricks","given":"E.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":147660,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kam, William","contributorId":85159,"corporation":false,"usgs":true,"family":"Kam","given":"William","email":"","affiliations":[],"preferred":false,"id":147661,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bowie, James E.","contributorId":29393,"corporation":false,"usgs":true,"family":"Bowie","given":"James","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":147659,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}