{"pageNumber":"411","pageRowStart":"10250","pageSize":"25","recordCount":10449,"records":[{"id":70010448,"text":"70010448 - 1962 - The solubility of quartz in water in the temperature interval from 25° to 300° C","interactions":[],"lastModifiedDate":"2015-06-22T09:01:28","indexId":"70010448","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","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":"The solubility of quartz in water in the temperature interval from 25° to 300° C","docAbstract":"

The solubility of quartz in water was investigated by three sets of experiments

\n
    \n
  1. at 1000 atm PH2O and temperatures ranging from 45° to 300°C
    2. \n
  2. at water pressures appropriate for the coexistence of three phases, gaseous water, liquid, and quartz, at temperatures ranging from 69° to 240°C
    3. \n
  3. a long term study of the dissolution of quartz grains which were continuously tumbled in water at room temperature.
    4. \n
\n

Saturated silica solutions in equilibrium with quartz were obtained in a few days at temperatures above 100°C. Equilibrium is shown by reproducible results for runs of different durations and by the precipitation of quartz from initially supersaturated solutions. The differential heat of solution derived from the data obtained at 1000 atm pressure is 5.38 kcal/mole.

\n

At room temperature and pressure, highly supersaturated silica solutions were obtained by continuously rotating quartz grains and water in plastic bottles at 75 rev/min. In one run the amount of silica in solution increased to a maximum value of 395 p.p.m. after 370 days. Another run reached 80 p.p.m. silica after 386 days and then dropped to 6 p.p.m. silica. It is concluded that quartz was precipitated at room temperature from this supersaturated solution and that 6 p.p.m. is essentially the true solubility of quartz at 25°C.

\n

In contrast to the runs rotated at 75 rev/min, quartz grains, and also silica glass grains, continuously rotated in water at\"\" rev/min, each contributed less than 1 p.p.m. colorimetric silica into solution after 1 year. Thus, vigorous agitation of the liquid is necessary to remove dissolved silica from the vicinity of surfaces of both quartz and glass.

\n

Two significant factors that may have contributed to the formation of supersaturated silica solutions in the runs rotated at 75 rev/min at room temperature are

\n
    \n
  1. stresses and structural irregularities at the surfaces of the crushed quartz grains, which contributed silica into solution more readily than well crystallized quartz
    2. \n
  2. the very slow rate at which dissolved silica polymerizes to species appropriate to act as nuclei for quartz growth. At the termination of the runs rotated at 75 rev/min, spikelike projections were present on many of the quartz grains. These are interpreted as indicating that abrasion was not the dominant cause for the great supersaturations which were obtained.
    3. \n
\n

 

","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(62)90027-3","issn":"00167037","usgsCitation":"Morey, G., Fournier, R., and Rowe, J., 1962, The solubility of quartz in water in the temperature interval from 25° to 300° C: Geochimica et Cosmochimica Acta, v. 26, no. 10, p. 1029-1040, https://doi.org/10.1016/0016-7037(62)90027-3.","productDescription":"12 p.","startPage":"1029","endPage":"1040","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":218798,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"26","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb043e4b08c986b324d40","contributors":{"authors":[{"text":"Morey, G.W.","contributorId":108155,"corporation":false,"usgs":true,"family":"Morey","given":"G.W.","email":"","affiliations":[],"preferred":false,"id":358950,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Fournier, R.O.","contributorId":73584,"corporation":false,"usgs":true,"family":"Fournier","given":"R.O.","email":"","affiliations":[],"preferred":false,"id":358949,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rowe, J.J.","contributorId":29460,"corporation":false,"usgs":true,"family":"Rowe","given":"J.J.","affiliations":[],"preferred":false,"id":358948,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70010741,"text":"70010741 - 1962 - The detection of sulphur in contamination spots in electron probe X-ray microanalysis","interactions":[],"lastModifiedDate":"2012-03-12T17:18:16","indexId":"70010741","displayToPublicDate":"1962-01-01T00:00:00","publicationYear":"1962","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1081,"text":"British Journal of Applied Physics","active":true,"publicationSubtype":{"id":10}},"title":"The detection of sulphur in contamination spots in electron probe X-ray microanalysis","docAbstract":"Sulphur has been identified as one of the elements present in the contamination spot which forms under the electron beam in the microprobe. The presence of the sulphur results in a rapid change in intensity measurements causing a loss of observed intensity for elements other than sulphur. The source of sulphur has been traced at least in part to the Apiezon B diffusion pump oil. A comparative X-ray fluorescence study of the Apiezon B and Octoil diffusion pump oils showed substantial amounts of sulphur in the Apiezon B. The Octoil was relatively free of sulphur.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"British Journal of Applied Physics","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1088/0508-3443/13/5/314","issn":"05083443","usgsCitation":"Adler, I., Dwornik, E., and Rose, H.J., 1962, The detection of sulphur in contamination spots in electron probe X-ray microanalysis: British Journal of Applied Physics, v. 13, no. 5, p. 245-246, https://doi.org/10.1088/0508-3443/13/5/314.","startPage":"245","endPage":"246","numberOfPages":"2","costCenters":[],"links":[{"id":204957,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1088/0508-3443/13/5/314"},{"id":219634,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"13","issue":"5","noUsgsAuthors":false,"publicationDate":"2002-11-20","publicationStatus":"PW","scienceBaseUri":"505baa94e4b08c986b3228bc","contributors":{"authors":[{"text":"Adler, I.","contributorId":13371,"corporation":false,"usgs":true,"family":"Adler","given":"I.","email":"","affiliations":[],"preferred":false,"id":359539,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dwornik, E.J.","contributorId":99128,"corporation":false,"usgs":true,"family":"Dwornik","given":"E.J.","email":"","affiliations":[],"preferred":false,"id":359541,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rose, H. J. Jr.","contributorId":79465,"corporation":false,"usgs":true,"family":"Rose","given":"H.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":359540,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":71747,"text":"tei791 - 1961 - Geologic summary of the Appalachian basin, with reference to the subsurface disposal of radioactive waste solutions","interactions":[],"lastModifiedDate":"2018-10-03T09:25:01","indexId":"tei791","displayToPublicDate":"2013-07-16T09:38:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":337,"text":"Trace Elements Investigations","code":"TEI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"791","title":"Geologic summary of the Appalachian basin, with reference to the subsurface disposal of radioactive waste solutions","docAbstract":"

The Appalachian basin is an elongate depression in the crystalline basement complex which contains a great volume of predominantly sedimentary stratified rocks. As defined in this paper it extends from the Adirondack Mountains in New York to central Alabama. From east to west it extends from the west flank of the Blue Ridge Mountains to the crest of the Findlay and Cincinnati arches and the Nashville dome. It encompasses an area of about 207,000 square miles, including all of West Virginia and parts of New York, New Jersey, Pennsylvania, Ohio, Maryland, Virginia, Kentucky, Tennessee, North Carolina, Georgia, and Alabama.

The stratified rocks that occupy the basin constitute a wedge-shaped mass whose axis of greatest thickness lies close to and parallel to the east edge of the basin. The maximum thickness of stratified rocks preserved in any one part of the basin today is between 35,000 and 40,000 feet. The volume of the sedimentary rocks is approximately 510,000 cubic miles and of volcanic rocks is a few thousand cubic miles. The sedimentary rocks are predominantly Paleozoic in age, whereas the volcanic rocks are predominantly Late Precambrian.

On the basis of gross lithology the stratified rocks overlying the crystalline basement complex can be divided into nine vertically sequential units, which are designated \"sequences\" in this report. The boundaries between contiguous sequences do not necessarily coincide with the commonly recognized boundaries between systems or series. All sequences are grossly wedge shaped, being thickest along the eastern margin of the basin and thinnest along the western margin.

The lowermost unit the Late Precambrian stratified sequence is present only along part of the eastern margin of the basin, where it lies unconformably on the basement complex. It consists largely of volcanic tuffs and flows but contains some interbedded sedimentary rocks. The Late Precambrian sequence is overlain by the Early Cambrian clastic sequence. Where the older sequence is absent, the Early Cambrian sequence rests on the basement complex. Interbedded fine- to coarse-grained noncarbonate detrital rocks comprise the bulk of the sequence, but some volcanic and carbonate rocks are included. Next above is the Cambrian-Ordovician carbonate sequence which consists largely of limestone and dolomite. Some quartzose sandstone is present in the lower part in the western half of the basin, and much shale is present in the upper part in the southeast part of the basin. The next higher sequence is the Late Ordovician clastic sequence, which consists largely of shale, siltstone, and sandstone. Coarse-grained light-gray to red rocks are common in the sequence along the eastern side of the basin, whereas fine-grained dark-gray to black calcareous rocks are common along the west side. The Late Ordovician clastic sequence is overlain unconformably in many places by the Early Silurian clastic sequence. The latter comprises a relatively thin wedge of coarse-grained clastic rocks. Some of the most prolific oil- and gas-producing sandstones in the Appalachian basin are included. Among these are the \"Clinton\" sands of Ohio, the Medina Sandstones of New York and Pennsylvania, and the Keefer or \"Big Six\" Sandstone of West Virginia and Kentucky. Conformably overlying the Early Silurian clastic sequence is the Silurian-Devonian carbonate sequence, which consists predominantly of limestone and dolomite. It also contains a salt-bearing unit in the north-central part of the basin and a thick wedge of coarse-grained red beds in the northeastern part. The sequence is absent in much of the southern part of the basin. Large volumes of gas and much oil are obtained from some of its rocks, especially from the Oriskany Sandstone and the Huntersville Ghert. The Silurian-Devonian carbonate sequence is abruptly overlain by the Devonian clastic sequence a thick succession of interbedded shale, mudrock, siltstone, and sandstone. Colors range from predominantly purple and red in the northeastern part of the basin to predominantly dark gray and black in the southwestern part. Many rocks in the upper part contain hydrocarbons in commercial quantities. The next higher sequence is a heterogeneous succession that comprises most rocks of Mississippian age in the basin. It is composed largely of fine-grained to very coarse-grained noncalcareous clastic rocks in the northern half of the basin, and largely of carbonate rocks in the southern part. Large quantities of oil and gas are produced from the sequence. The youngest sequence consists of coarse-grained clastic rocks largely of Pennsylvanian age. In the center of the basin a relatively small volume of lithologically similar rocks of Permian age are included. The sequence has been intensively mined for coal throughout most of its extent.

The waste-disposal possibilities of the stratified rocks in the Appalachian basin are considered in terms of the following: 1) gross lithology of the sequences; 2) general lithology of the rock units composing the sequences; and 3) the structural attitudes of the sequences in different parts of the basin. The degree of exploitation of economically significant mineral* resources is considered briefly where such exploitation may affect waste-disposal possibilities. Hydrologic aspects are not in general considered. Based largely on consideration of the above geologic factors the following types of reservoirs associated with particular geologic environments offer some prospects for the disposal of radioactive waste solutions. They are: 1) artificially created cavities in thick salt beds; 2) artificially fractured thin lenticular sandstone bodies isolated in shale or mudrock sequences; 3) portions of thick noncarbonate clastic sequences possessing appreciable natural porosity and permeability; 4) thin clastic units (with natural or artificially created openings) in the plate of a thrust fault overlain by impermeable strata.

Considered in its entirety the Late Ordovician clastic sequence appears to have a greater number of favorable geologic factors for waste-disposal purposes than the others. The Early Silurian clastic sequence, the Silurian-Devonian carbonate sequence, and the Devonian clastic sequence offer fewer possibilities. The Late Precambrian stratified sequence, Early Cambrian, and the Cambrian-Ordovician carbonate sequence offer few possibilities. The Mississippian and Pennsylvanian sequences appear to be generally unsuitable.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/tei791","collaboration":"Prepared on behalf of the U.S. Atomic Energy Commission","usgsCitation":"Colton, G.W., 1961, Geologic summary of the Appalachian basin, with reference to the subsurface disposal of radioactive waste solutions: U.S. Geological Survey Trace Elements Investigations 791, Report: 121 p.; 15 Maps; 1 Illustration, https://doi.org/10.3133/tei791.","productDescription":"Report: 121 p.; 15 Maps; 1 Illustration","costCenters":[],"links":[{"id":358066,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358065,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0028/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358067,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358068,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358069,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358070,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358071,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358072,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358073,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358074,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358075,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358076,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358077,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358078,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358079,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358080,"rank":17,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":358081,"rank":18,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":290249,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0028/report-thumb.jpg"}],"country":"United States","otherGeospatial":"Appalachian Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.71,35.8 ], [ -84.71,43.91 ], [ -74.13,43.91 ], [ -74.13,35.8 ], [ -84.71,35.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53c79ef3e4b0194841642446","contributors":{"authors":[{"text":"Colton, George Willis","contributorId":12015,"corporation":false,"usgs":true,"family":"Colton","given":"George","email":"","middleInitial":"Willis","affiliations":[],"preferred":false,"id":284696,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":52228,"text":"ofr6228 - 1961 - Geologic summary of the Appalachian Basin, with reference to the subsurface disposal of radioactive waste solutions","interactions":[],"lastModifiedDate":"2018-10-03T09:24:58","indexId":"ofr6228","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"62-28","title":"Geologic summary of the Appalachian Basin, with reference to the subsurface disposal of radioactive waste solutions","docAbstract":"

The Appalachian basin is an elongate depression in the crystalline basement complex which contains a great volume of predominantly sedimentary stratified rocks. As defined in this paper it extends from the Adirondack Mountains in New York to central Alabama. From east to west it extends from the west flank of the Blue Ridge Mountains to the crest of the Findlay and Cincinnati arches and the Nashville dome. It encompasses an area of about 207,000 square miles, including all of West Virginia and parts of New York, New Jersey, Pennsylvania, Ohio, Maryland, Virginia, Kentucky, Tennessee, North Carolina, Georgia, and Alabama.

The stratified rocks that occupy the basin constitute a wedge-shaped mass whose axis of greatest thickness lies close to and parallel to the east edge of the basin. The maximum thickness of stratified rocks preserved in any one part of the basin today is between 35,000 and 40,000 feet. The volume of the sedimentary rocks is approximately 510,000 cubic miles and of volcanic rocks is a few thousand cubic miles. The sedimentary rocks are predominantly Paleozoic in age, whereas the volcanic rocks are predominantly Late Precambrian.

On the basis of gross lithology the stratified rocks overlying the crystalline basement complex can be divided into nine vertically sequential units, which are designated \"sequences\" in this report. The boundaries between contiguous sequences do not necessarily coincide with the commonly recognized boundaries between systems or series. All sequences are grossly wedge shaped, being thickest along the eastern margin of the basin and thinnest along the western margin.

The lowermost unit the Late Precambrian stratified sequence is present only along part of the eastern margin of the basin, where it lies unconformably on the basement complex. It consists largely of volcanic tuffs and flows but contains some interbedded sedimentary rocks. The Late Precambrian sequence is overlain by the Early Cambrian clastic sequence. Where the older sequence is absent, the Early Cambrian sequence rests on the basement complex. Interbedded fine- to coarse-grained noncarbonate detrital rocks comprise the bulk of the sequence, but some volcanic and carbonate rocks are included. Next above is the Cambrian-Ordovician carbonate sequence which consists largely of limestone and dolomite. Some quartzose sandstone is present in the lower part in the western half of the basin, and much shale is present in the upper part in the southeast part of the basin. The next higher sequence is the Late Ordovician clastic sequence, which consists largely of shale, siltstone, and sandstone. Coarse-grained light-gray to red rocks are common in the sequence along the eastern side of the basin, whereas fine-grained dark-gray to black calcareous rocks are common along the west side. The Late Ordovician clastic sequence is overlain unconformably in many places by the Early Silurian clastic sequence. The latter comprises a relatively thin wedge of coarse-grained clastic rocks. Some of the most prolific oil- and gas-producing sandstones in the Appalachian basin are included. Among these are the \"Clinton\" sands of Ohio, the Medina Sandstones of New York and Pennsylvania, and the Keefer or \"Big Six\" Sandstone of West Virginia and Kentucky. Conformably overlying the Early Silurian clastic sequence is the Silurian-Devonian carbonate sequence, which consists predominantly of limestone and dolomite. It also contains a salt-bearing unit in the north-central part of the basin and a thick wedge of coarse-grained red beds in the northeastern part. The sequence is absent in much of the southern part of the basin. Large volumes of gas and much oil are obtained from some of its rocks, especially from the Oriskany Sandstone and the Huntersville Ghert. The Silurian-Devonian carbonate sequence is abruptly overlain by the Devonian clastic sequence a thick succession of interbedded shale, mudrock, siltstone, and sandstone. Colors range from predominantly purple and red in the northeastern part of the basin to predominantly dark gray and black in the southwestern part. Many rocks in the upper part contain hydrocarbons in commercial quantities. The next higher sequence is a heterogeneous succession that comprises most rocks of Mississippian age in the basin. It is composed largely of fine-grained to very coarse-grained noncalcareous clastic rocks in the northern half of the basin, and largely of carbonate rocks in the southern part. Large quantities of oil and gas are produced from the sequence. The youngest sequence consists of coarse-grained clastic rocks largely of Pennsylvanian age. In the center of the basin a relatively small volume of lithologically similar rocks of Permian age are included. The sequence has been intensively mined for coal throughout most of its extent.

The waste-disposal possibilities of the stratified rocks in the Appalachian basin are considered in terms of the following: 1) gross lithology of the sequences; 2) general lithology of the rock units composing the sequences; and 3) the structural attitudes of the sequences in different parts of the basin. The degree of exploitation of economically significant mineral* resources is considered briefly where such exploitation may affect waste-disposal possibilities. Hydrologic aspects are not in general considered. Based largely on consideration of the above geologic factors the following types of reservoirs associated with particular geologic environments offer some prospects for the disposal of radioactive waste solutions. They are: 1) artificially created cavities in thick salt beds; 2) artificially fractured thin lenticular sandstone bodies isolated in shale or mudrock sequences; 3) portions of thick noncarbonate clastic sequences possessing appreciable natural porosity and permeability; 4) thin clastic units (with natural or artificially created openings) in the plate of a thrust fault overlain by impermeable strata.

Considered in its entirety the Late Ordovician clastic sequence appears to have a greater number of favorable geologic factors for waste-disposal purposes than the others. The Early Silurian clastic sequence, the Silurian-Devonian carbonate sequence, and the Devonian clastic sequence offer fewer possibilities. The Late Precambrian stratified sequence, Early Cambrian, and the Cambrian-Ordovician carbonate sequence offer few possibilities. The Mississippian and Pennsylvanian sequences appear to be generally unsuitable.

","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ofr6228","collaboration":"Prepared on behalf of the U.S. Atomic Energy Commission","usgsCitation":"Colton, G.W., 1961, Geologic summary of the Appalachian Basin, with reference to the subsurface disposal of radioactive waste solutions: U.S. Geological Survey Open-File Report 62-28, Report: 121 p.; 15 Maps; 1 Illustration, https://doi.org/10.3133/ofr6228.","productDescription":"Report: 121 p.; 15 Maps; 1 Illustration","costCenters":[],"links":[{"id":86729,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86730,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":177170,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1962/0028/report-thumb.jpg"},{"id":86731,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86732,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86733,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86734,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86735,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86736,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86737,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86738,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86739,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86740,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86741,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86742,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86743,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86744,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1962/0028/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":86745,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1962/0028/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","otherGeospatial":"Appalachian Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.71,35.8 ], [ -84.71,43.91 ], [ -74.13,43.91 ], [ -74.13,35.8 ], [ -84.71,35.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db688132","contributors":{"authors":[{"text":"Colton, George Willis","contributorId":12015,"corporation":false,"usgs":true,"family":"Colton","given":"George","email":"","middleInitial":"Willis","affiliations":[],"preferred":false,"id":244999,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1260,"text":"wsp1534 - 1961 - Progress report on wells penetrating artesian aquifers in South Dakota","interactions":[{"subject":{"id":55762,"text":"ofr5732 - 1957 - Records of selected artesian wells in South Dakota","indexId":"ofr5732","publicationYear":"1957","noYear":false,"title":"Records of selected artesian wells in South Dakota"},"predicate":"SUPERSEDED_BY","object":{"id":1260,"text":"wsp1534 - 1961 - Progress report on wells penetrating artesian aquifers in South Dakota","indexId":"wsp1534","publicationYear":"1961","noYear":false,"title":"Progress report on wells penetrating artesian aquifers in South Dakota"},"id":1}],"lastModifiedDate":"2016-04-05T09:41:30","indexId":"wsp1534","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1534","title":"Progress report on wells penetrating artesian aquifers in South Dakota","docAbstract":"

Artesian aquifers underlie most of South Dakota and large areas in adjacent States. About 15,000 wells have been completed since 1881 in these aquifers within South Dakota. Many wells that originally flowed have ceased to flow and have been abandoned, and others have been equipped with pumps. Many thousands, however, continue to flow. This report presents data collected through June 1958 and includes records of 1,045 flowing and nonflowing artesian wells

\n

Sufficient information is not available at present (1958) to permit a detailed description of the geologic and hydrologic properties of artesian aquifers or their correlation in South Dakota. The description of the various aquifers given in this report is, therefore, necessarily a general one.

","language":"English","publisher":"U.S. Government Print Office","doi":"10.3133/wsp1534","usgsCitation":"Davis, R.W., Dyer, C., and Powell, J., 1961, Progress report on wells penetrating artesian aquifers in South Dakota: U.S. Geological Survey Water Supply Paper 1534, Report: iv, 100 p.; 3 Plates: 26.00 x 17.50 inches or smaller, https://doi.org/10.3133/wsp1534.","productDescription":"Report: iv, 100 p.; 3 Plates: 26.00 x 17.50 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":137430,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1534/report-thumb.jpg"},{"id":26208,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1534/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26209,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1534/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26210,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1534/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":26211,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1534/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -104.029541015625,\n 45.935870621190546\n ],\n [\n -104.08447265624999,\n 43.004647127794435\n ],\n [\n -98.536376953125,\n 42.99661231842139\n ],\n [\n -98.031005859375,\n 42.74701217318067\n ],\n [\n -97.811279296875,\n 42.85180609584705\n ],\n [\n -97.23999023437499,\n 42.85180609584705\n ],\n [\n -96.976318359375,\n 42.73894375124379\n ],\n [\n -96.624755859375,\n 42.569264372193864\n ],\n [\n -96.40502929687499,\n 42.21224516288584\n ],\n [\n -96.317138671875,\n 42.25291778330197\n ],\n [\n -96.40502929687499,\n 42.39912215986002\n ],\n [\n -96.45996093749999,\n 42.553080288955826\n ],\n [\n -96.64672851562499,\n 42.73087427928485\n ],\n [\n -96.5478515625,\n 42.84375132629021\n ],\n [\n -96.492919921875,\n 43.03677585761058\n ],\n [\n -96.427001953125,\n 43.15710884095329\n ],\n [\n -96.51489257812499,\n 43.29320031385282\n ],\n [\n -96.51489257812499,\n 43.381097587278596\n ],\n [\n -96.602783203125,\n 43.50872101129684\n ],\n [\n -96.448974609375,\n 43.492782808225\n ],\n [\n -96.43798828125,\n 45.24395342262324\n ],\n [\n -96.51489257812499,\n 45.38301927899065\n ],\n [\n -96.64672851562499,\n 45.40616374516014\n ],\n [\n -96.778564453125,\n 45.51404592560424\n ],\n [\n -96.866455078125,\n 45.63708709571876\n ],\n [\n -96.624755859375,\n 45.767522962149904\n ],\n [\n -96.56982421875,\n 45.94351068030587\n ],\n [\n -104.029541015625,\n 45.935870621190546\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9ae4b07f02db65d9f3","contributors":{"authors":[{"text":"Davis, R. W.","contributorId":93459,"corporation":false,"usgs":true,"family":"Davis","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":143456,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dyer, C.F.","contributorId":23917,"corporation":false,"usgs":true,"family":"Dyer","given":"C.F.","email":"","affiliations":[],"preferred":false,"id":143454,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Powell, J.E.","contributorId":27030,"corporation":false,"usgs":true,"family":"Powell","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":143455,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70220645,"text":"70220645 - 1961 - Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming","interactions":[],"lastModifiedDate":"2021-05-21T19:21:30.166576","indexId":"70220645","displayToPublicDate":"1961-12-31T14:17:30","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming","docAbstract":"

Normal faults offset a bedrock surface scoured by Pleistocene ice in several areas within and south of Yellowstone National Park. Recurrent earthquake shocks and fresh appearance of some scarps suggest that movement is continuing along some faults. Four systems of faults are described. Quaternary movement occurred along more than 60 faults on the Mirror Plateau, 15 miles northeast of Yellowstone Lake. Faults trend northwest, and several are more than 6 miles long. Maximum displacement exceeds 250 feet. The majority have northeast blocks downdropped, but some grabens and horsts are present. Eocene to Pliocene igneous or pyroclastic rocks are displaced. Ice moved southwest and south from the Beartooth and Absaroka ranges, nearly at right angles to the fault trends. Drainage in many ice-scoured valleys was disrupted by faulting, and small lakes (such as Mirror Lake) formed on downthrown blocks. Thermal activity occurs along some of these faults. Directly east of Mirror Plateau, the Lamar normal fault has a displacement of 1300 + feet; perhaps 1000 feet of this may have occurred during Quaternary time. The Yellowstone Falls fault system cuts Pliocene rhyolite southeast of the Upper Falls of the Yellowstone River. Faults trend northwest; maximum displacement exceeds 200 feet. The Solfatara fault system trends north-northwest, cuts Pliocene rhyolite, and has a maximum Quaternary displacement of about 200 feet. The Hering Lake fault system is a northern extension of the Teton fault, trends northward, and cuts Pliocene rhyolite and rhyolitic welded tuff. Maximum displacement is about 200 feet. West-flowing streams established on bedrock scoured by ice were disrupted, and Beula, Hering, and South Boundary lakes formed on the downthrown (east) blocks. The sharp angular unstepped appearance of fault scarps 50 to 200 feet high in these fault systems suggests that each scarp of this type was formed by one continuous movement. The displacement along faults associated with the Hebgen earthquake of August 1959 is commonly less than 20 feet. The abundance of Quaternary faults and the record of 18 earthquakes in historic time suggest that additional faulting and earthquake activity can be expected in the future. Recognition of this probability should influence the location and type of construction of buildings and other facilities. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1749:RSOQFI]2.0.CO;2","usgsCitation":"Love, D., 1961, Reconnaissance study of quaternary faults in and south of Yellowstone National Park, Wyoming: Geological Society of America Bulletin, v. 72, no. 12, p. 1749-1764, https://doi.org/10.1130/0016-7606(1961)72[1749:RSOQFI]2.0.CO;2.","productDescription":"16 p.","startPage":"1749","endPage":"1764","costCenters":[],"links":[{"id":480377,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://figshare.com/articles/figure/Reconnaissance_study_of_Quaternary_faults_in_and_south_of_Yellowstone_National_Park_Wyoming/13687621","text":"External Repository"},{"id":385865,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wyoming","otherGeospatial":"Yellowstone National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.03881835937499,\n 43.6599240747891\n ],\n [\n -108.797607421875,\n 43.6599240747891\n ],\n [\n -108.797607421875,\n 45.01141864227728\n ],\n [\n -111.03881835937499,\n 45.01141864227728\n ],\n [\n -111.03881835937499,\n 43.6599240747891\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Love, D.","contributorId":15809,"corporation":false,"usgs":true,"family":"Love","given":"D.","email":"","affiliations":[],"preferred":false,"id":816284,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220644,"text":"70220644 - 1961 - Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana","interactions":[],"lastModifiedDate":"2021-05-21T19:16:21.510182","indexId":"70220644","displayToPublicDate":"1961-12-31T14:08:45","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana","docAbstract":"

Douglass Creek basin lies west of the Continental Divide in the northern part of the Rocky Mountain physiographic province. Numerous minor environmental differences exist between the Douglass Creek area and the Pipestone Springs and Canyon Ferry areas east of the Divide. In the 19th century, however, the three areas had identical mammalian species representation, although not equally dense populations. Fossils of an early Oligocene biota have been collected from the Douglass Creek basin. Presence of all but one of the Douglass Creek mammalian species in the Pipestone Springs-Canyon Ferry early Oligocene fauna suggests that the three ancient ecosystems resembled each other in much the same way as the 19th century systems. The early Oligocene deposits and biota of the Douglass Creek basin indicate a moist, temperate climate with seasonal variations. Sediment size and distribution suggest that the cross-valley relief was no greater than it is now. The fish and invertebrate faunas show that a shallow, hard-water lake existed in the area. The flora included a lowland, lake-border association and an upland coniferous forest. Although the ancient Douglass Creek biota doubtless included many species not represented in the fossil collections, most of the mammalian species are probably represented in the combined Douglass Creek, Pipestone Springs, and Canyon Ferry fossil assemblages. If so, the number of mammalian species was about the same as in the 19th century ecosystem.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1633:POAEOB]2.0.CO;2","usgsCitation":"Konizeski, R.L., 1961, Paleoecology of an early oligocene biota from Douglass Creek Basin, Montana: Geological Society of America Bulletin, v. 72, no. 11, p. 1633-1642, https://doi.org/10.1130/0016-7606(1961)72[1633:POAEOB]2.0.CO;2.","productDescription":"10 p.","startPage":"1633","endPage":"1642","costCenters":[],"links":[{"id":385864,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","otherGeospatial":"Douglas Creek","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -113.06510925292969,\n 46.584350070440536\n ],\n [\n -112.91130065917969,\n 46.584350070440536\n ],\n [\n -112.91130065917969,\n 46.62963563393178\n ],\n [\n -113.06510925292969,\n 46.62963563393178\n ],\n [\n -113.06510925292969,\n 46.584350070440536\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Konizeski, Richard L.","contributorId":80248,"corporation":false,"usgs":true,"family":"Konizeski","given":"Richard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":816283,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220634,"text":"70220634 - 1961 - An aeromagnetic profile from anchorage to Nome, Alaska","interactions":[],"lastModifiedDate":"2021-05-21T17:35:10.663879","indexId":"70220634","displayToPublicDate":"1961-12-31T12:31:47","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"An aeromagnetic profile from anchorage to Nome, Alaska","docAbstract":"

A total-intensity profile was obtained on a 500-mile flight by a U. S. Geological Survey airplane from Anchorage to Nome, Alaska, on May 4, 1954. The average flight altitude was 6,000 ft above sea level except over the Alaska Range where the flight altitude was 9,000 ft. This profile crossed eight of the major tectonic elements of Alaska at right angles to their trend and gives valuable regional information in an area where other geophysical and geological information is scarce or lacking. The profile has a net gradient downward to the northwest, most of which is ascribed to the component of the earth's main magnetic field along the flight traverse. The great variety of magnetic anomalies which are superimposed on this gradient originate from variations in lithology along the traverse. All the magnetic anomalies, except a large one over the Yukon River, are caused by magnetic rocks at or near the surface. The magnetic profile may be divided into four major segments and nine subsegments, each having a characteristic magnetic pattern. Most of these can be related to a tectonic unit. The large plutons of the Talkeetna geanticline are clearly defined by a group of anomalies having the highest amplitudes of any on the profile. The Matanuska geosyncline to the east is represented by a 25-mile section of sloping profile consistent with a thick sedimentary section but indicating that the geosyncline is comparatively narrow near Anchorage. The 200-mile central magnetic segment is relatively free from all but very minor anomalies. This segment includes the Alaska Range geosyncline, the Tanana geanticline, and the Kuskokwim geosyncline; showing only slight magnetic contrasts between each of these elements. The two geosynclines either have thick Mesozoic sedimentary sections or have underlying crystalline rocks which are low in magnetic susceptibility at shallow depths. The rocks of the geanticline have a low but not negligible magnetic susceptibility and are predominantly Paleozoic sedimentary rocks. A single 300-gamma anomaly on the west edge of the central segment is caused by a small, mafic intrusive body in the Paleozoic metamorphic rocks of Mt. Hurst. West of this anomaly the profile consists of a series of small sharp anomalies which are probably caused by Paleozoic metavolcanic rocks of the Ruby geanticline. The second largest anomaly on the profile is in the Koyukuk geosyncline over the Yukon River. The source is calculated to be more than a mile deep and may be an intrusive body at least 15 miles wide. This anomaly is flanked by 20-mile sections of flat or sloping profile which indicate areas of thick sedimentary rocks, particularly in the region west of the Yukon River. The 150-mile Norton Sound magnetic segment on the western end of the profile consists of many closely spaced anomalies produced by rocks which are either volcanic or similar to the Seward complex. Of the four Cenozoic basins or lowlands crossed by the profile, three are underlain by rocks of moderate to high magnetic susceptibility at shallow depths. These are the Cook Inlet basin, part of which overlaps rocks of the Talkeetna geanticline, the Innoko basin of central Alaska which overlies the rocks of the Ruby geanticline, and the Norton basin, in which sedimentary deposits are thin or absent. The fourth, the Minchumina basin, is underlain by the low-susceptibility rocks at the Tanana geanticline, which are also probably close to the surface. 

","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1438945","usgsCitation":"King, E.R., 1961, An aeromagnetic profile from anchorage to Nome, Alaska: Geophysics, v. 26, no. 6, p. 716-726, https://doi.org/10.1190/1.1438945.","productDescription":"11 p.","startPage":"716","endPage":"726","costCenters":[],"links":[{"id":385854,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","city":"Nome","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -166.46484375,\n 63.97596090918338\n ],\n [\n -163.740234375,\n 63.97596090918338\n ],\n [\n -163.740234375,\n 65.10914820386473\n ],\n [\n -166.46484375,\n 65.10914820386473\n ],\n [\n -166.46484375,\n 63.97596090918338\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"26","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"King, E. R.","contributorId":93482,"corporation":false,"usgs":true,"family":"King","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":816264,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220620,"text":"70220620 - 1961 - Local evidence of Pleistocene to recent orogeny in the Argentine Andes","interactions":[],"lastModifiedDate":"2021-05-21T15:04:09.046919","indexId":"70220620","displayToPublicDate":"1961-12-31T09:57:21","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":"Local evidence of Pleistocene to recent orogeny in the Argentine Andes","docAbstract":"

Deformed continental sedimentary rocks are exposed in the province of Salta, northwestern Argentina, in one of many intermontane basins of the Puna, a high desert region of subparallel north-trending block-fault ranges. These rocks, formerly thought to be Tertiary but recently dated by fossil diatoms as Pleistocene or younger, comprise several thousand feet of elastics and evaporites interpreted as having accumulated in a structural basin under geologic and climatic conditions much like those of today. They are overlain unconformably by sedimentary rocks and sediments of three distinct depositional periods. The stratigraphic section is as follows: Fan gravels and playa deposits (Recent) - Disconformity - Flat-lying lacustrine sandstones and siltstones, minor salines - Angular unconformity - Gently folded conglomerates and sandstones - Angular unconformity - Folded and faulted conglomerate, sandstone, shale, evaporites, and tuffs The basin rocks are folded along north-trending axes and are cut by northeast- to southeast-trending normal faults and by a north-trending reverse fault; the next younger conglomerates and sandstones are gently folded; the two youngest units are undisturbed. The three unconformities, the faults and folds in the older beds, and post-lake-bed faulting of an erosion surface on an adjacent block all indicate intermittent late Pleistocene to Recent local deformation. Neither regional tension nor regional compression can explain both the Pleistocene to Recent movements on the regional block faults and the contemporaneous compressional structures within the basin. The mechanism of horst-wedging, suggested by a current explanation of the analogous ranges of the Great Basin, is proposed as a solution to the dilemma; the horst blocks, forced directly upward along Miocene normal faults, acted as wedges and compressed the sediments accumulating in the graben, creating the pattern of faults and folds now observed. If such structures are ever discovered in the North American Great Basin, as seems reasonable, they should offer new insight into the understanding of basin-and-range structure. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1539:LEOPTR]2.0.CO;2","usgsCitation":"Pratt, W.P., 1961, Local evidence of Pleistocene to recent orogeny in the Argentine Andes: Bulletin of the Geological Society of America, v. 72, no. 10, p. 1539-1550, https://doi.org/10.1130/0016-7606(1961)72[1539:LEOPTR]2.0.CO;2.","productDescription":"12 p.","startPage":"1539","endPage":"1550","costCenters":[],"links":[{"id":385838,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Argentina","otherGeospatial":"Andes Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -68.53271484375,\n -32.34284135639302\n ],\n [\n -64.62158203125,\n -32.34284135639302\n ],\n [\n -64.62158203125,\n -25.045792240303435\n ],\n [\n -68.53271484375,\n -25.045792240303435\n ],\n [\n -68.53271484375,\n -32.34284135639302\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Pratt, Walden P.","contributorId":68296,"corporation":false,"usgs":true,"family":"Pratt","given":"Walden","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":816242,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220630,"text":"70220630 - 1961 - Late quaternary history of the snake river in the American Falls region, Idaho","interactions":[],"lastModifiedDate":"2021-05-21T16:41:02.448609","indexId":"70220630","displayToPublicDate":"1961-12-01T11:34:23","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":"Late quaternary history of the snake river in the American Falls region, Idaho","docAbstract":"

While mapping the American Falls region, we found evidence that contributes to the middle Pleistocene to Recent history of the Snake River, and indirectly to the history of overflow of Lake Bonneville. Middle Pleistocene to recent rocks in the valley are mainly lacustrine and fluvial silts and clays, with some sand, gravel, basalt, and a few thin tuff beds. The formation of terraces can be correlated with events both up- and downstream.

The Snake River was at least once, and possibly twice, dammed and diverted by eruptions of basalt, resulting in the formation of lakes and deposition of lacustrine beds. A rather flat-lying, thin, but persistent gravel at the base of one lake bed formation may represent a glacial period, possibly Illinoian, during which the Snake River had a large volume.

Overflow of water from Lake Bonneville into the Snake River system, by way of the Marsh Creek-Portneuf valley, laid down a deltaic-fluvial deposit here named the Michaud Gravel. At this time the Snake River, greatly augmented by Lake Bonneville overflow, began to cut channels through and around a lava dam. Terraces between Aberdeen, American Falls, and Pocatello were formed during the existence of the lake in which the Michaud Gravel was deposited and by fluvial processes after drainage of the lake. At one stage in the downcutting, bars of huge basalt boulders were built across the mouths of abandoned spillways.

Radiocarbon dating and geologic evidence from the area between Preston and Soda Springs, Idaho, suggest that basalt flows diverted the Bear River into Lake Bonneville, perhaps causing it to overflow. This diversion probably occurred about 33,000 years ago. This dating accords with events in the American Falls region.

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1961)72[1739:LQHOTS]2.0.CO;2","usgsCitation":"Trimble, D.E., and Carr, W.J., 1961, Late quaternary history of the snake river in the American Falls region, Idaho: Bulletin of the Geological Society of America, v. 72, no. 12, p. 1739-1748, https://doi.org/10.1130/0016-7606(1961)72[1739:LQHOTS]2.0.CO;2.","productDescription":"10 p.","startPage":"1739","endPage":"1748","costCenters":[],"links":[{"id":385850,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho","otherGeospatial":"Snake River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.82861328125001,\n 42.407234661551875\n ],\n [\n -111.29150390625,\n 42.407234661551875\n ],\n [\n -111.29150390625,\n 45.19752230305682\n ],\n [\n -116.82861328125001,\n 45.19752230305682\n ],\n [\n -116.82861328125001,\n 42.407234661551875\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"72","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Trimble, Donald E.","contributorId":75910,"corporation":false,"usgs":true,"family":"Trimble","given":"Donald","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":816259,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carr, Wilfred James","contributorId":12033,"corporation":false,"usgs":true,"family":"Carr","given":"Wilfred","email":"","middleInitial":"James","affiliations":[],"preferred":false,"id":816260,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70171262,"text":"70171262 - 1961 - Use of water-well data in interpreting occurrence of aquifers in northeastern Lyon County, Minnesota","interactions":[],"lastModifiedDate":"2018-03-19T11:11:05","indexId":"70171262","displayToPublicDate":"1961-07-12T10:00:00","publicationYear":"1961","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Use of water-well data in interpreting occurrence of aquifers in northeastern Lyon County, Minnesota","docAbstract":"

In northeastern Lyon County the areal distribution of aquifers of Cretaceous age determined from well-bottom altitudes suggests a series of interbedded sandstones striking northwestward and overlapping one another to the northeast. Probably the numerous thin sandstone aquifers in the area were deposited near the flanks of a Precambrian granite “high” area by a transgressing Late Cretaceous sea.

","language":"English","publisher":"Geological Society of America","publisherLocation":"Boulder, CO","doi":"10.1130/0016-7606(1961)72[1275:UOWDII]2.0.CO;2","usgsCitation":"Rodis, H.G., 1961, Use of water-well data in interpreting occurrence of aquifers in northeastern Lyon County, Minnesota: GSA Bulletin, v. 72, p. 1275-1278, https://doi.org/10.1130/0016-7606(1961)72[1275:UOWDII]2.0.CO;2.","productDescription":"4 p.","startPage":"1275","endPage":"1278","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":321704,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Minnesota","county":"Lyon County","volume":"72","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57481e3ee4b07e28b664dc1a","contributors":{"authors":[{"text":"Rodis, Harry G.","contributorId":25141,"corporation":false,"usgs":true,"family":"Rodis","given":"Harry","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":630359,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220641,"text":"70220641 - 1961 - Tephroite in California manganese deposits","interactions":[],"lastModifiedDate":"2021-05-21T18:49:23.59965","indexId":"70220641","displayToPublicDate":"1961-01-01T13:45:05","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":"Tephroite in California manganese deposits","docAbstract":"

Recent studies of manganese deposits and mineral specimens in the Sierran belt of sedimentary rocks as well as in the Klamath Mountains to the north and in the Rand Mountains to the south, have shown the presence of tephroite, the orthosilicate of manganese (Mn2Si04), at numerous localities. Earlier studies of these deposits have shown that the original layered deposits of carbonate and hydrous silicates of manganese have been widely altered by metamorphism to spessartite (Mn3Al2-(SiO.),), rhodonite (MnSi03), and piedmontite (Ca2(Al,Mn\"',Fe\"')3-Si3Oi2(OH)). Recent work shows that layered manganese oxides also were present in the original sedimentary rocks. It shows also, that tephroite has formed widely in the original assemblage of carbonate, silicate, and oxide of manganese; in several localities, a little alleghanyite (2Mn2-S1O4 - Mn(OH,F)2) has been formed. Rhodonite, spessartite, and piedmontite uniformly follow the tephroite; in places, bementite and neotocite are present. In one deposit a little pyroxmangite ( (Mn,Fe,Ca)Si03) has been noted and in another, some crystals that are probably pyrophanite (MnTi03), not yet recorded in the United States. By contrast, the restudy of large collections of material from deposits in sedimentary rocks of the Franciscan formation in the Coast Ranges indicates the tephroite is very uncommon; it has been recognized with assurance at only one locality-Alum Rock Park, Santa Clara County. In the Coast Ranges, rhodonite and spessartite, the high manganese garnet, are very uncommon. The assemblages of manganese silicates indicate that the layered deposits of manganese minerals in the Sierra belt have been metamorphosed to a higher degree than those of the Coast Ranges. This review also shows the presence of axinite, the boro-silicate of aluminum, calcium, and manganese, in three deposits.

","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/GSECONGEO.56.1.39","usgsCitation":"Hewett, D.F., Chesterman, C.W., and Troxel, B., 1961, Tephroite in California manganese deposits: Economic Geology, v. 56, no. 1, p. 39-58, https://doi.org/10.2113/GSECONGEO.56.1.39.","productDescription":"20 p.","startPage":"39","endPage":"58","costCenters":[],"links":[{"id":385861,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.99267578124999,\n 42.01665183556825\n ],\n [\n -124.25537109375,\n 42.00032514831621\n ],\n [\n -124.4091796875,\n 40.53050177574321\n ],\n [\n -123.74999999999999,\n 38.77121637244273\n ],\n [\n -120.673828125,\n 34.43409789359469\n ],\n [\n -118.91601562499999,\n 32.1570124860701\n ],\n [\n -117.24609374999999,\n 32.54681317351514\n ],\n [\n -114.6533203125,\n 32.7872745269555\n ],\n [\n -114.3896484375,\n 32.89803818160521\n ],\n [\n -114.10400390625,\n 34.34343606848294\n ],\n [\n -114.63134765625001,\n 35.06597313798418\n ],\n [\n -119.72900390625001,\n 38.87392853923629\n ],\n [\n -119.99267578124999,\n 42.01665183556825\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"56","issue":"1","noUsgsAuthors":false,"publicationDate":"1961-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hewett, D. F.","contributorId":19927,"corporation":false,"usgs":true,"family":"Hewett","given":"D.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":816272,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Chesterman, C. W.","contributorId":115850,"corporation":false,"usgs":true,"family":"Chesterman","given":"C.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":816273,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Troxel, B.W.","contributorId":101681,"corporation":false,"usgs":true,"family":"Troxel","given":"B.W.","email":"","affiliations":[],"preferred":false,"id":816274,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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":70010751,"text":"70010751 - 1961 - Aqua de Ney, California, a spring of unique chemical character","interactions":[],"lastModifiedDate":"2020-11-16T17:46:55.379168","indexId":"70010751","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":"Aqua de Ney, California, a spring of unique chemical character","docAbstract":"

The chemistry of water of Aqua de Ney, a cold spring of unusual character located in Siskiyou County, Calif., has been re-examined as part of a study of the relation of water chemistry to rock environment. The water has a pH of 11·6 and a silica content of 4000 parts per million (p.p.m.), the highest values known to occur in natural ground waters.

The rocks exposed nearby consist of two volcanic sequences, one predominantly basaltic in composition, the other highly siliceous. Neither these rocks nor the sedimentary and igneous rocks presumed to underlie the area at depth seem to offer explanation of the unusual mineralization which includes 240 p.p.m. of boron, 1000 p.p.m. of sulphide (as H2S), and 148 p.p.m. of ammonia nitrogen (as NH4) in a water that is predominantly sodium chloride and sodium carbonate in character.

By analogy, it is assumed that water from Aqua de Ney is the product of an initial mixture of connate sea water with a calcium magnesium sulphate water. It is postulated that ion exchange has increased the content of sodium and reduced that of calcium and magnesium, and that sulphate reduction has brought about the high alkalinity, high pH, and high content of sulphide. The large silica value is explained as the result of solution of silica by water having the high pH observed.

","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(61)90107-7","usgsCitation":"Feth, J.H., Rogers, S.M., and Roberson, C.E., 1961, Aqua de Ney, California, a spring of unique chemical character: Geochimica et Cosmochimica Acta, v. 22, no. 2-4, p. 75-86, https://doi.org/10.1016/0016-7037(61)90107-7.","productDescription":"14 p.","startPage":"75","endPage":"86","costCenters":[],"links":[{"id":219639,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","county":"Siskiyou County","otherGeospatial":"Aqua de Ney Spring","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.32119798660277,\n 41.26464643600054\n ],\n [\n -122.29740142822266,\n 41.26464643600054\n ],\n [\n -122.29740142822266,\n 41.26977529310511\n ],\n [\n -122.32119798660277,\n 41.26977529310511\n ],\n [\n -122.32119798660277,\n 41.26464643600054\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"22","issue":"2-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ed03e4b0c8380cd49589","contributors":{"authors":[{"text":"Feth, J. H.","contributorId":50495,"corporation":false,"usgs":true,"family":"Feth","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":359567,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rogers, S. M.","contributorId":101637,"corporation":false,"usgs":true,"family":"Rogers","given":"S.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":359568,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Roberson, C. E.","contributorId":40190,"corporation":false,"usgs":true,"family":"Roberson","given":"C.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":359566,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"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; Pb206U238&lt;Pb207U235&#x2AA1;Pb207Pb206\">Pb206U238<Pb207U235⪡Pb207Pb206 or, less frequently, Pb207Pb206&#x2AA1;Pb207U235&lt;Pb206U238\">Pb207Pb206⪡Pb207U235<Pb206U238. These discordant age sequences have been attributed most often to uncertainties in the common lead correction, selective loss of radio-active daughter products, loss or gain of lead or uranium, or contamination by an older generation of radiogenic lead.

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 Pb206U238\">Pb206U238 (N206N238\">N206N238) vs. radiogenic Pb207U235\">Pb207U235 (N207N235\">N207N235) after correcting for the contaminating common Pb206 and Pb207. The linear relationships noted in this graphical procedure have been extended to plots of the mole ratios of total Pb206U238\">Pb206U238 (tN206N238\">tN206N238) vs. total Pb207U235\">Pb207U235 (tN207N235\">tN207N235). This modification permits the calculation of concordant ages for unaltered samples using only the Pb207Pb206\">Pb207Pb206 ratio of the contaminating common lead.

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[(N206N204)x &#x2212; (N206N204)y(N238N204)x &#x2212;(N238N204)y] vs. [(N207N204)x &#x2212; (N207N204)y(N235N204)x &#x2212;(N235N204)y]\">[(N206N204)x − (N206N204)y(N238N204)x −(N238N204)y] vs. [(N207N204)x − (N207N204)y(N235N204)x −(N235N204)y] can give concordant ages corrected for unknown amounts of a common lead with an unknown Pb207/ Pb206 ratio. (If thorium is absent the difference ratios may be normalized with the more abundant index isotope, Pb208.) Similar plots of tho normalized, difference ratios for three genetically related samples (x − y) and(x − z), will give concordant ages corrected, in addition, for either one unknown period of past alteration or initial contamination by an older generation of radiogenic lead of unknown Pb207/Pb206 ratio.

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":70161053,"text":"70161053 - 1960 - A statistical analysis of the distribution of a larval nematode (Anisakis sp.) in the musculature of chum salmon (Oncorhynchus keta - Walbaum)","interactions":[],"lastModifiedDate":"2016-01-05T08:46:42","indexId":"70161053","displayToPublicDate":"2015-10-12T05:15:00","publicationYear":"1960","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1609,"text":"Experimental Parasitology","active":true,"publicationSubtype":{"id":10}},"title":"A statistical analysis of the distribution of a larval nematode (Anisakis sp.) in the musculature of chum salmon (Oncorhynchus keta - Walbaum)","docAbstract":"

The pepsin-HCl digestion technique is probably the best method of isolating Anisakislarvae from the musculature of chum salmon. Some losses can be expected due to breakage of the resistant cuticle of Anisakis, and can be estimated to be about 6% when counting the parasites with the unaided eye.

\n
Comparisons of Anisakis infections of the dorsal and ventral musculature indicated that very few larvae are found in the dorsal portions (above the lateral line). Forty-seven per cent of the fish had no dorsal infections, and 90% of the fish had less than 10% of total infection in the dorsal musculature.
\n
Comparisons of Anisakis infection ratios of the right and left sides below the lateral line showed some variation. Chi-square tests of the hypothesis that 50% of the infections occur in either side indicated no significant differences. There were indications that large total infection intensities displayed less variation.
\n
Comparisons of Anisakis infections of the anterior and posterior portions of the lateral musculature indicated that the infections were greater in the anterior portions. Calculated 95% confidence limits showed 50.0 to 59.0% infection in the anterior portion compared to 41.0 to 50.0% in the posterior portion.
\n
Analyses of the Anisakis distributions within the anterior portions of the lateral musculature were hindered by extreme variation in the counts. In general, an average of 60% of the anterior portion infections occurred in the upper two quadrants of musculature, and 40% in the lower two quadrants. Changes in distributional patterns were affected by total parasite density, rather than by age or geographical location.
\n
For purposes of comparing infection rates in chum salmon, distributional patterns indicate that the minimum sample of musculature which should be taken from each fish is one side below the lateral line.
\n
The one factor which probably contributes the greatest effect on distributional patterns of Anisakis within chum salmon musculature is the total intensity of infection (or population density of Anisakis) in each fish.
","language":"English","publisher":"Elselvier","doi":"10.1016/0014-4894(60)90062-X","usgsCitation":"Novotny, A., 1960, A statistical analysis of the distribution of a larval nematode (Anisakis sp.) in the musculature of chum salmon (Oncorhynchus keta - Walbaum): Experimental Parasitology, v. 10, no. 2, p. 60-67, https://doi.org/10.1016/0014-4894(60)90062-X.","productDescription":"8 p.","startPage":"60","endPage":"67","numberOfPages":"8","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":313291,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"10","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"568cf73be4b0e7a44bc0f12d","contributors":{"authors":[{"text":"Novotny, A.J.","contributorId":112643,"corporation":false,"usgs":true,"family":"Novotny","given":"A.J.","email":"","affiliations":[],"preferred":false,"id":584515,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2338,"text":"wsp1487 - 1960 - Geology and ground-water resources of the lower Little Bighorn River Valley, Big Horn County, Montana, with special reference to the drainage of waterlogged lands","interactions":[],"lastModifiedDate":"2023-07-18T10:57:54.875188","indexId":"wsp1487","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1487","title":"Geology and ground-water resources of the lower Little Bighorn River Valley, Big Horn County, Montana, with special reference to the drainage of waterlogged lands","docAbstract":"

The lower Little Bighorn River valley, Montana, is in the unglaciated part of the Missouri Plateau section of the Great Plains physiographic province. The river and its principal tributaries rise in the Bighorn Mountains, and the confluence of this northward-flowing stream with the Bighorn River is near the east edge of Hardin, Mont. The normal annual precipitation ranges from about 12 inches in the northern part of the area to 15 inches in the southern part. The economy of the area is founded principally on farming, much of the low-lying land adjacent to the river being irrigated. The irrigated land is within the Crow Indian Reservation, although a part is privately owned. The bedrock formations exposed in the area are of Cretaceous age and include the Parkman sandstone, Claggett shale, Eagle sandstone, Telegraph Creek shale, and Cody shale. The Cloverly formation, Tensleep sandstone, and Madison limestone, which underlie but are not exposed in the area, and the Parkman sandstone in the southern half of the area appear to be the principal bedrock aquifers. All except the Parkman lie at depths ranging from a few feet to several thousand feet, and all appear to be capable of yielding water in commercial quantities. Some of the other formations arc capable of yielding enough water for domestic and stock needs. The river alluvium of Recent age and the Pleistocene terrace deposits are the principal unconsolidated formations in the area with respect to water supply and drainage. Wells yielding as much as 100 gallons per minute may be developed in favorable areas. Pumping tests reveal that the transmissibility of the coarser unconsolidated materials probably ranges from about 15,000 to 30,000 gallons per day per foot. Two tests of the Parkman sandstone showed transmissibilities of 6,000 and 20,000 gallons per day per foot. Although a test of the Cloverly formation showed a transmissibility of only 3,000 gallons per day per foot, the high artesian pressure--80 pounds per square inch at the land surface--in the Cloverly caused the tested well to yield about 200 gallons per minute by natural flow; this is greater than the yield of any other single well in the area. Textural properties were compared with the hydraulic properties determined by laboratory tests to show the relation between different types of waterbearing materials. Materials classified as heavy soils-normally somewhat dense and impervious-had an average permeability of 7.2 gallons per day per square foot, which was more than expected. One sample of very coarse alluvial material had a permeability of 6,000 gallons per day per square foot. The depth to water beneath irrigation units was mapped, thus showing the waterlogged areas. Waterlogging is not a serious problem where the water table is more than 6 feet below the land surface. For the drainage studies the unconsolidated deposits are classified in two zones-coarse-grained sediments resting on the relatively impermeable bedrock floor and overlying fine-grained sediments which extend to the land surface. The transmissibility of the coarse-sediment zone generally is many times greater than that of the fine-sediment zone. Because in many places drains could not be economically dug deep enough to enter the coarse zone, the study of the effectiveness of drainage completed in the fine zone received much attention. The studies showed that, despite a considerable thickness of fine-grained sediments between the bottom of the drain and the top of the coarse zone, drainage ditches frequently were effective in relieving waterlogging of fields nearby. Pilot relief wells installed in existing drains showed that the effectiveness of some drains could be increased appreciably by installing a series of relief wells. Records of fluctuations of water levels in 196 observation wells and water-level contour maps were studied to show the principal areas of recharge and discharge in the irrigable areas. 

","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1487","usgsCitation":"Moulder, E.A., Klug, M.F., Morris, D.A., Swenson, F.A., and Krieger, R.A., 1960, Geology and ground-water resources of the lower Little Bighorn River Valley, Big Horn County, Montana, with special reference to the drainage of waterlogged lands: U.S. Geological Survey Water Supply Paper 1487, Report: viii, 223 p.; 13 Plates: 17.00 × 42.65 inches or smaller, https://doi.org/10.3133/wsp1487.","productDescription":"Report: viii, 223 p.; 13 Plates: 17.00 × 42.65 inches or smaller","costCenters":[],"links":[{"id":28222,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28221,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28217,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28216,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28215,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28214,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28213,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":396137,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_24428.htm"},{"id":28223,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1487/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138575,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1487/report-thumb.jpg"},{"id":28210,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28211,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28212,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28218,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28219,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":28220,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1487/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Montana","county":"Big Horn County","otherGeospatial":"lower Little Bighorn River Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -107.529,\n 45.266\n ],\n [\n -107.338,\n 45.266\n ],\n [\n -107.338,\n 45.72\n ],\n [\n -107.529,\n 45.72\n ],\n [\n -107.529,\n 45.266\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db68530a","contributors":{"authors":[{"text":"Moulder, E. A.","contributorId":78719,"corporation":false,"usgs":true,"family":"Moulder","given":"E.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":145043,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Klug, M. F.","contributorId":97372,"corporation":false,"usgs":true,"family":"Klug","given":"M.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":145044,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Morris, D. A.","contributorId":56204,"corporation":false,"usgs":true,"family":"Morris","given":"D.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":145041,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Swenson, F. A.","contributorId":71622,"corporation":false,"usgs":true,"family":"Swenson","given":"F.","email":"","middleInitial":"A.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":145042,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Krieger, R. A.","contributorId":11202,"corporation":false,"usgs":true,"family":"Krieger","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":145040,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"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":70220592,"text":"70220592 - 1960 - A comprehensive system of automatic computation in magnetic and gravity interpretation","interactions":[],"lastModifiedDate":"2021-05-20T19:20:02.92688","indexId":"70220592","displayToPublicDate":"1960-12-31T14:15:30","publicationYear":"1960","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"A comprehensive system of automatic computation in magnetic and gravity interpretation","docAbstract":"

In the interpretation of magnetic and gravity anomalies, downward continuation of fields and calculation of first and second vertical derivatives of fields have been recognized as effective means for bringing into focus the latent diagnostic features of the data. A comprehensive system has been devised for the calculation of any or all of these derived fields on modern electronic digital computing equipment. The integral for analytic continuation above the plane is used with a Lagrange extrapolation polynomial to derive a general determinantal expression from which the field at depth and the various derivatives on the surface and at depth can be obtained. It is shown that the general formula includes as special cases some of the formulas appearing in the literature. The process involves a \"once for all depths\" summing of grid values on a system of concentric circles about each point followed by application of the appropriate one or more of the 19 sets of coefficients derived for the purpose. Theoretical and observed multilevel data are used to illustrate the processes and to discuss the errors. The coefficients can be used for less extensive computations on a desk calculator. 

","language":"English","publisher":"Society of Exploration Geophysicists","doi":"10.1190/1.1438736","usgsCitation":"Henderson, R., 1960, A comprehensive system of automatic computation in magnetic and gravity interpretation: Geophysics, v. 25, no. 3, p. 569-585, https://doi.org/10.1190/1.1438736.","productDescription":"17 p.","startPage":"569","endPage":"585","costCenters":[],"links":[{"id":385806,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"25","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Henderson, R.G.","contributorId":72521,"corporation":false,"usgs":true,"family":"Henderson","given":"R.G.","email":"","affiliations":[],"preferred":false,"id":816107,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220533,"text":"70220533 - 1960 - Foothills fault system, western Sierra Nevada, California","interactions":[],"lastModifiedDate":"2021-05-18T17:31:01.879116","indexId":"70220533","displayToPublicDate":"1960-12-31T12:27:00","publicationYear":"1960","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":"Foothills fault system, western Sierra Nevada, California","docAbstract":"

A large fault system, here named the Foothills fault system, is the dominant structural feature of the western Sierra Nevada. The steeply dipping to vertical component faults trend northwestward through an area about 200 miles long and 30 miles wide north of 37°30' north latitude. The faulted Paleozoic and Mesozoic rocks are overlapped by unfaulted younger rocks, and the total extent of the fault system is not known. It is probably not limited to the western Sierra Nevada. Faults are marked by belts as much as 4 miles wide of cataclastically deformed and recrystallized rocks and by truncated folds. Along one fault, Upper Jurassic rocks are juxtaposed against Paleozoic rocks for at least 100 miles. The direction of fault movement has not been determined. Net displacement on some of the component faults exceeds 3000 feet and may be measurable in miles. Major faults cut beds of Late Jurassic age and are in turn cut by plutonic rocks of probable Late Jurassic and Middle Cretaceous age. Faults that controlled deposition of quartz veins and gold ore bodies of the Mother Lode belt are apparently younger and structurally less important features superimposed on one of the fault zones of the large system. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)71[483:FFSWSN]2.0.CO;2","usgsCitation":"Clark, L.D., 1960, Foothills fault system, western Sierra Nevada, California: Bulletin of the Geological Society of America, v. 71, no. 4, p. 483-496, https://doi.org/10.1130/0016-7606(1960)71[483:FFSWSN]2.0.CO;2.","productDescription":"14 p.","startPage":"483","endPage":"496","costCenters":[],"links":[{"id":385720,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Sierra Nevada Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.025390625,\n 36.70365959719456\n ],\n [\n -117.75146484375,\n 36.70365959719456\n ],\n [\n -117.75146484375,\n 39.232253141714885\n ],\n [\n -121.025390625,\n 39.232253141714885\n ],\n [\n -121.025390625,\n 36.70365959719456\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Clark, L. D.","contributorId":11189,"corporation":false,"usgs":true,"family":"Clark","given":"L.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":815910,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220580,"text":"70220580 - 1960 - Geology of the Mayagüez area, Puerto Rico","interactions":[],"lastModifiedDate":"2021-05-19T15:12:37.584864","indexId":"70220580","displayToPublicDate":"1960-12-31T10:07:45","publicationYear":"1960","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":"Geology of the Mayagüez area, Puerto Rico","docAbstract":"

The Mayagüez area forms the southwestern corner of Puerto Rico, west of 67° W. and south of 18° 15' N. One-third of the 640 square kms is covered by thick alluvium. Unconformities separate a basal complex, two sequences of highly folded igneous and sedimentary rocks, and a younger sequence of gently dipping sedimentary rock. The basal Bermeja complex contains serpentinite, silicified porphyritic volcanic rock with some sedimentary rock, and minor spilite, amphibolitized spilite, and amphibolite. It is exposed chiefly in some anticlinal cores in southwestern Puerto Rico. Limestone, mudstone, andesite, and basalt form the older folded sequence. The Río Loco formation, bronzite andesite porphyry in part with pillow structures, was extruded perhaps in the Cenomanian. The Mayagüez group includes most of the rocks in southwestern Puerto Rico: the Yauco mudstone, Parguera limestone, Brujo limestone, Melones limestone, Maricao basalt, Sabana Grande andesite, and El Rayo volcanic rocks. The maximum possible age range is Turonian to Maestrichtian. The group ranges in thickness from about 800 m in the south to 3800 m in the north, and it varies in lithology from limestone in the south to mudstone and volcanic rock in the north, indicating a volcanic center to the north during that time. The second folded sequence contains andesitic volcanic rock, bedded tuff, and massive limestone. The San Germán formation (Maestrichtian) includes andesite, the Cabo Rojo agglomerate member, and the Cotui limestone member. The Jicara formation, massive limestone and bedded tuff, is Paleocene; there is one exposure of an unnamed ? Eocene marl. Post-Eocene limestone and conglomerate are also exposed in the area. The structure of the basement complex is obscured by its massiveness and by the cover of younger rocks. Two major deformations have affected the rocks of southwestern Puerto Rico since Cenomanian to Santonian time. In the Maestrichtian, the first of these formed folds with a N. 60° W. trend, asymmetric or overturned to the south. Near the south coast the folding of thin Mayagüez group rocks was probably influenced by trends in the Bermeja complex which caused deviations in the regional trends and also some overturning to the north. The San Germán formation, deposited unconformably on the eroded surface of the folded Mayagüez group, contains large allochthonous blocks of older and contemporaneous rocks. These blocks, up to 2 km by 1 km in exposure, were deposited by slumping or sliding due to gravity within and at the base and top of the San Germán formation near Lajas and San Germán. Most rocks in the blocks are extremely contorted and contain deformed Foraminifera. The San Germán and Jicara formations and perhaps the ?Eocene marls were deformed into gentle open folds trending east in the area covered by this report. Oligocene, Miocene, and younger sedimentary rocks have been tilted and uplifted. Large east-west left-lateral transcurrent faults cross the area, offsetting and offset by two sets of transverse faults (N. 45° E., N. 20° W.): most faults are probably Maestrichtian to Oligocene, although minor faulting has continued to the present. Dikes and sills of quartz diorite porphyry and mica-quartz dacite porphyry intrude the ?Maestrichtian San Germán formation and older units. A diorite plug cuts the Bermeja complex, and a granodiorite plug intrudes the Mayagüez group. 

","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)71[319:GOTMAP]2.0.CO;2","usgsCitation":"Mattson, P.H., 1960, Geology of the Mayagüez area, Puerto Rico: Bulletin of the Geological Society of America, v. 71, no. 3, p. 319-362, https://doi.org/10.1130/0016-7606(1960)71[319:GOTMAP]2.0.CO;2.","productDescription":"44 p.","startPage":"319","endPage":"362","costCenters":[],"links":[{"id":385772,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Puerto Rico","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -67.52197265625,\n 17.832374329567518\n ],\n [\n -65.302734375,\n 17.832374329567518\n ],\n [\n -65.302734375,\n 18.58377568837094\n ],\n [\n -67.52197265625,\n 18.58377568837094\n ],\n [\n -67.52197265625,\n 17.832374329567518\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Mattson, Peter H.","contributorId":72659,"corporation":false,"usgs":true,"family":"Mattson","given":"Peter","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":816069,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220495,"text":"70220495 - 1960 - The chief oxide-burgin area discoveries, East Tintic district, Utah; A case history","interactions":[],"lastModifiedDate":"2021-05-17T13:54:52.042882","indexId":"70220495","displayToPublicDate":"1960-11-01T08:47:35","publicationYear":"1960","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":"The chief oxide-burgin area discoveries, East Tintic district, Utah; A case history","docAbstract":"

In 1955 exploration for base and precious metals was undertaken by Bear Creek Mining Company immediately north of the Main Tintic district, Utah. During the course of this work Bear Creek became interested in the East Tintic district, primarily as a result of the activities of the U.S. Geological Survey in that area. Data published on the East Tintic district by the Survey and others were studied and map data made available from various mining companies were compiled. Preliminary economic studies were made to determine the present day value of the type of ore body discovered previously in the district. Encouraging results from these investigations led to the selection of specific targets for exploration. Recommendations for a project program were made and approved. Negotiations were successfully concluded in mid-1956 for a unit lease agreement on lands in the East Tintic district owned by the Tintic Standard and Chief Consolidated mining companies and their subsidiaries. Of the targets selected for exploration, the Chief Oxide area seemed to be one of the most prominent. Our preliminary work in the Chief Oxide area corroborated the findings of the U.S. Geological Survey described in Part I of this paper. After careful consideration it was decided to gamble the cost of an exploration shaft in this area for the purpose of providing an underground drilling platform. We also hoped by means of underground workings to establish the existence and nature of the postulated fault. A limited amount of surface drilling was done prior to shaft sinking in order to locate a shaft site and also to obtain additional information of subvolcanic structure and alteration. Underground exploration in the Chief Oxide area was started in January, 1957. The Burgin shaft was sunk to a depth of 1,100 feet and by August, 1959, lateral development on the 1050 level totaled 4,721 feet and underground diamond drilling totaled 15,480 feet. Results of the work done to date are as follows: (a) Identification of the sedimentary rock section and an interpretation of the structure in the Burgin mine area. (b) Discovery by penetration of the previously postulated East Tintic thrust fault. (c) Discovery of large zones of manganese oxides and carbonates, which were found to be closely related to silver-lead-zinc mineralization. (d) Discovery of ore-grade lead-zinc mineralization within the footwall rocks of the East Tintic thrust. (e) Discovery of high-grade silver-lead ore within the thrust zone. Insofar as ore localization is concerned the most important structural feature in the Burgin mine area is the East Tintic thrust fault-a fact that opens up new ore potential over a large part of the East Tintic district not previously explored. Although the discoveries to date must be attributed essentially to the application of geology to exploration, the tools of geochemical prospecting and geophysics were also used, and the geochemical work, in particular, was found to be a definite aid in the selection of areas for further exploration.

","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.55.7.1507","usgsCitation":"Bush, J., Cook, D., Lovering, T.S., and Morris, H.T., 1960, The chief oxide-burgin area discoveries, East Tintic district, Utah; A case history: Economic Geology, v. 55, no. 7, p. 1507-1540, https://doi.org/10.2113/gsecongeo.55.7.1507.","productDescription":"34 p.","startPage":"1507","endPage":"1540","costCenters":[],"links":[{"id":385678,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Utah","otherGeospatial":"east Tintic Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.9287109375,\n 38.81831117374662\n ],\n [\n -110.8795166015625,\n 38.81831117374662\n ],\n [\n -110.8795166015625,\n 40.069664523297774\n ],\n [\n -111.9287109375,\n 40.069664523297774\n ],\n [\n -111.9287109375,\n 38.81831117374662\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"55","issue":"7","noUsgsAuthors":false,"publicationDate":"1960-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Bush, J.B.","contributorId":258145,"corporation":false,"usgs":false,"family":"Bush","given":"J.B.","email":"","affiliations":[],"preferred":false,"id":815769,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cook, D.R.","contributorId":20585,"corporation":false,"usgs":true,"family":"Cook","given":"D.R.","email":"","affiliations":[],"preferred":false,"id":815770,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lovering, T. S.","contributorId":108085,"corporation":false,"usgs":true,"family":"Lovering","given":"T.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":815771,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Morris, H. T.","contributorId":15585,"corporation":false,"usgs":true,"family":"Morris","given":"H.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":815772,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70221609,"text":"70221609 - 1960 - Deposits of the manganese oxides","interactions":[],"lastModifiedDate":"2021-06-29T13:23:55.213152","indexId":"70221609","displayToPublicDate":"1960-06-25T08:24:04","publicationYear":"1960","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":"Deposits of the manganese oxides","docAbstract":"

One of the problems of the wartime program of studies of domestic manganese deposits concerned the identification of, and modes of origin of the manganese oxide minerals. Of the hundreds of specimens of the oxides collected in the United States, the minerals of about 250 specimens were identified by X-ray analysis; complete chemical analyses were made of about 35 specimens and partial analyses of about 150 specimens. This report presents the conclusions that arise out of a review of the geologic environment under which the specimens were found. One conclusion of this review concerns the supergene vs. hypogene origin of the oxides. In order to reach conclusions concerning the supergene and hypogene origin of the 33 oxides of manganese recognized thus far, it was necessary to define the criteria that seemed usable.One group of oxides appears to be persistently supergene: groutite, hydrohausmannite, lithiophorite, rancieite, hetaerolite, hydrohetaerolite, chalcophanite, crednerite, woodruffite, and wad. Another group of oxides appears to have been formed only by hypogene processes: manganosite, hausmannite, pyrochroite, bixbyite, galaxite, jacobsite, franklinite, pyrophanite, and ilmenite. A third group of oxides appear to have been formed by supergene processes in some places and by hypogene processes in other places: manganite, pyrolusite, ramsdellite, cryptomelane, psilomelane, hollandite, braunite, and coronadite.Another conclusion concerns a genetic relation between: (1) veins of manganese oxides in the southwest, largely in Tertiary volcanic rocks, (2) bodies of oxides in travertine aprons near active hot springs, and inactive Pleistocene springs, and (3) stratified oxides, largely in late Tertiary sedimentary rocks in the southwest. From the features of these three groups of deposits of oxides and their geologic and geographic distribution, it appears that hot water from great depth rose on fractures in areas of volcanic activity, deposited oxides in the fractures, appeared at the surface as hot springs, deposited oxides in the aprons near the springs and continuing to local basins, deposited manganese oxides with local debris as persistent beds in sediments, partly or wholly of volcanic origin.

","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.55.1.1","usgsCitation":"Petersen, R.G., 1960, Deposits of the manganese oxides: Economic Geology, v. 55, no. 1, p. 1-55, https://doi.org/10.2113/gsecongeo.55.1.1.","productDescription":"55 p.","startPage":"1","endPage":"55","costCenters":[],"links":[{"id":386734,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"55","issue":"1","noUsgsAuthors":false,"publicationDate":"1960-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Petersen, Richard G.","contributorId":44232,"corporation":false,"usgs":true,"family":"Petersen","given":"Richard","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":818369,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70181751,"text":"70181751 - 1960 - Ground-water hydrology and glacial geology of the Kalamazoo area, Michigan","interactions":[],"lastModifiedDate":"2017-02-14T10:04:16","indexId":"70181751","displayToPublicDate":"1960-01-08T00:00:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":130,"text":"Progress Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"23","title":"Ground-water hydrology and glacial geology of the Kalamazoo area, Michigan","docAbstract":"

The Kalamazoo report area includes about 150 square miles of Kalamazoo County, Mich. The area is principally one of industry and commerce, although agriculture also is of considerable importance. It has a moderate and humid climate and lies within the Lake Michigan “snow belt”. Precipitation averages about 35 inches per year. Snowfall averages about 55 inches.

The surface features of the area were formed during and since the glacial epoch and are classified as outwash plain, morainal highlands, and glaciated channels or drainageways. The area is formed largely on the remnants of an extensive outwash plain, which is breached by the Kalamazoo River in the northeastern part and is dissected elsewhere by several small tributaries to the river. Most of the land drained by these tributaries lies within the report area. A small portion of the southern part drains to the St. Joseph River.

The Coldwater shale, which underlies the glacial deposits throughout the area, and the deeper bedrock formations are not tapped for water by wells and they have little or no potential for future development.

Deposits of glacial drift, which are the source of water to all the wells in the area, have considerable potential for future development. These deposits range in thickness from about 40 feet along the Kalamazoo River to 350 feet where valleys were eroded in the bedrock surface. Permeable outwash and channel deposits are the sources of water for wells of large capacity. The moraines are formed dominantly by till of lower permeability which generally yields small supplies of water, but included sand and gravel beds of higher permeability yield larger supplies locally.

The aquifers of the Kalamazoo area are recharged by infiltration of rainfall and snowmelt and by infiltration of surface waters induced by pumping of wells near the surface sources. Water pumped from most of the municipal well fields is replenished in part by such induced infiltration. Many of the industrial wells along the Kalamazoo River and Portage Creek are recharged in part from these streams. Locally, however, recharge from the streams is impeded, as their bottoms have become partly sealed by silt and solid waste matter.

Water levels fluctuate with seasonal and annual changes in precipitation and in response to pumping. Pumpage by the city of Kalamazoo increased from about 300 million gallons in 1880 to 4.6 billion gallons in 1957. Despite the fact that billions of gallons are pumped annually from well fields in the Axtell Creek area, water levels in this vicinity have declined only a few feet, as the discharge from the fields is approximately compensated by recharge from precipitation and surface water. Pumpage of ground water by industry in 1948 was estimated at about 14 billion gallons, but the use of ground water for industrial purposes has since declined.

Aquifer tests indicate that the coefficient of transmissibility of aquifers in the area ranges from as little as 18,000 to as high as 300,000 gpd (gallons per day) per foot, and that ground water occurs under watertable and artesian conditions.

The ground water is of the calcium magnesium bicarbonate type. It is generally hard to very hard and commonly contains objectionable amounts of iron. Locally, the water contains appreciable amounts of sulfate. Study of the chemical analyses of waters from the area show that all of the tributaries to the Kalamazoo River are fed primarily by ground-water discharge.

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