The eastern slope of Rocky Mountain National Park, Colorado, has been subjected to at least three separate Pleistocene glaciations, which from oldest to youngest are correlated with the Buffalo, Bull Lake, and Pinedale glaciations of Blackwelder in the Wind River Mountains of Wyoming. In this area, deposits of the oldest glaciation are known from only one locality. Deposits of the Bull Lake glaciation comprise two sets of moraines indicative of two advances of ice separated by a significant recession; those of the Pinedale glaciation comprise three sets of moraines indicative of a maximum advance of the ice and two recessional halts or minor readvances. Moraines of two minor advances of the ice, correlated with the Temple Lake and historic stades of Neoglaciation in the Wind River Mountains, occur in the cirque heads.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)71[1371:GOTESO]2.0.CO;2","usgsCitation":"Richmond, G.M., 1960, Glaciation of the east slope of Rocky Mountain National Park, Colorado: Bulletin of the Geological Society of America, v. 71, no. 9, p. 1371-1382, https://doi.org/10.1130/0016-7606(1960)71[1371:GOTESO]2.0.CO;2.","productDescription":"12 p.","startPage":"1371","endPage":"1382","costCenters":[],"links":[{"id":385718,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Rocky Mountain National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106.051025390625,\n 40.16208338164617\n ],\n [\n -105.4193115234375,\n 40.16208338164617\n ],\n [\n -105.4193115234375,\n 40.58267063809529\n ],\n [\n -106.051025390625,\n 40.58267063809529\n ],\n [\n -106.051025390625,\n 40.16208338164617\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Richmond, Gerald M","contributorId":127101,"corporation":false,"usgs":true,"family":"Richmond","given":"Gerald","email":"","middleInitial":"M","affiliations":[],"preferred":false,"id":815908,"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":70221796,"text":"70221796 - 1960 - The chief oxide-burgin area discoveries, East Tintic district, Utah; A case history","interactions":[],"lastModifiedDate":"2021-07-07T12:28:44.400442","indexId":"70221796","displayToPublicDate":"1960-07-07T07:25:53","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":"The Burgin shaft is in the Chief Oxide area of the E. Tintic district, Utah, and is about a mile E. of any previously known ore bodies; workings from it are currently developing a substantial amount of commercial Pb-Zn ore in several blind ore bodies that lie in folded Paleozoic carbonate rock concealed beneath a blanket of Eocene lava. This area was mapped by Tower and Smith of the U.S. Geological Survey in 1897 and again by Lindgren and Loughlin in 1911, but no detailed work was done until after 1943 when a field party headed by T.S. Lovering began a study of the entire E. Tintic district. The history of the development of exploration concepts is summarized under Historical Summary. The E. Tintic mining district is in the E.-central part of a N.-trending fault-block mountain range near the eastern margin of the Great Basin; dominant structures of the range are a N.-trending syncline on the W. and a less well exposed anticline on the E. Both folds are cut by an intersecting system of transcurrent strike-slip faults and by minor thrust faults and normal faults of moderate displacement. A strong W.-dipping thrust fault cuts the anticline a short distance E. of the fold axis, but is hidden by Eocene lava throughout the E. Tintic district. The pre-Tertiary rocks range from Lower Cambrian to Upper Mississippian and exceed 7,000 ft. in total thickness; they are dominantly marine limestone and dolomite except for a thick basal Cambrian quartzite. The Tertiary rocks are chiefly dacitic lavas and pyroclastic deposits that are intruded by moderately persistent dikes and irregular bodies of monzonite and quartz porphyry. Nearly all the faulting and folding took place before the extrusion of the lavas on a rugged Eocene erosion surface. At about the time of the intrusion of monzonitic magma, many of the faults in the Paleozoic rock were re-opened and in the overlying lava some fracturing took place which was later accented by hydrothermal alteration. Most of the ore mined in the E. Tintic district has come from Pb-Zn-Ag replacement bodies in shattered Jasperoidized hydrothermal dolomite at the intersection of low angle faults and steep mineralized NE.-trending cross fractures. The U.S. Geological Survey studies of 1943 to 1957 concentrated on detailed mapping of geology and alteration in the E. Tintic district, together with field and laboratory studies of the relation of alteration to stages of mineralization and ore deposition. Trenching and core drilling were carried on after World War II to aid in interpreting the subrhyolite geology, and the Chief Oxide area was 1 of 4 localities tested by drilling. Study of the fossils, lithology, and alteration shown here in a deep drill core, together with the knowledge of the regional geology, led to an essentially correct interpretation of subrhyolite structure in the strongly discordant underlying Paleozoic rocks in which a mineralized tear fault cuts a strong thrust fault, and to the conclusion that ore stage mineralization was present in substantial amounts in the Paleozoic rocks below the Chief Oxide alteration patch in the quartz latite lava. Subsequent geothermal and geochemical work strengthened this conclusion, and the recent development work of the Bear Creek Mining Company, which sank the Burgin shaft, has shown the presence of Pb-Zn-Ag ore of commercial grade in substantial amount in blind ore bodies below the lava blanket in the Chief Oxide area.
No abstract available.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)10[1541:SOTQAE]2.0.CO;2","usgsCitation":"Scott, G., 1960, Subdivision of the quaternary alluvium east of the front range near Denver, Colorado: GSA Bulletin, v. 71, no. 10, p. 1541-1544, https://doi.org/10.1130/0016-7606(1960)10[1541:SOTQAE]2.0.CO;2.","productDescription":"4 p.","startPage":"1541","endPage":"1544","costCenters":[],"links":[{"id":375978,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","city":"Denver","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.66650390625,\n 38.34165619279595\n ],\n [\n -104.447021484375,\n 38.34165619279595\n ],\n [\n -104.447021484375,\n 40.863679665481676\n ],\n [\n -105.66650390625,\n 40.863679665481676\n ],\n [\n -105.66650390625,\n 38.34165619279595\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Scott, Glenn R.","contributorId":33324,"corporation":false,"usgs":true,"family":"Scott","given":"Glenn R.","affiliations":[],"preferred":false,"id":791695,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220589,"text":"70220589 - 1960 - Stratigraphic and geotectonic relationships in northern Vermont and southern Quebec","interactions":[],"lastModifiedDate":"2021-05-20T18:49:24.731852","indexId":"70220589","displayToPublicDate":"1960-05-01T13:42:52","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":"Stratigraphic and geotectonic relationships in northern Vermont and southern Quebec","docAbstract":"Stratified rocks of early and middle Paleozoic age form a belt of northeast-trending anticlinoria and synclinoria of middle Paleozoic age, in northern Vermont and adjacent parts of southern Quebec. The foreland margin of this belt, in the Champlain and St. Lawrence valleys to the west, is cut by eastward-dipping thrust faults of middle Paleozoic age and by later northeast-trending normal faults. The Green Mountain anticlinorium, which is the dominant structure of the region, is flanked to the west, on the foreland, by the St. Albans-Hinesburg-Middlebury synclinorium and to the east, in the midst of the folded belt, by the Connecticut Valley-Gaspe synclinorium. The principal thrust faults, notably the Champlain and Philipsburg thrusts, are in the west limb of the St. Albans-Hinesburg-Middlebury synclinorium. East of the Connecticut Valley-Gaspe synclinorium is the Boundary Mountain anticlinorium, in eastern Vermont and adjacent New Hampshire and along the international boundary between Quebec and Maine. Two contrasting intergradational lithic assemblages, the graywacke-shale assemblage and the carbonate-quartzite assemblage, characterize the protolith of the bedded rocks. The graywacke-shale assemblage includes thick sections of lower Paleozoic strata, portions of which lap both gradationally and unconformably westward on the foreland, particularly in Quebec; it also includes middle Paleozoic strata that offlap eastward away from the foreland. The carbonate-quartzite assemblage laps both unconformably and gradationally eastward over the graywacke-shale assemblage in sections of the middle Paleozoic east of the axis of the Green Mountain anticlinorium. Stratigraphic correlation has become well established in the foreland belt where numerous distinctive and fossiliferous strata, chiefly of the carbonate-quartzite assemblage, have escaped metamorphism. It is also fairly clear in sections in the eastern foreland and western part of the Green Mountain anticlinorium, where the strata of the carbonate-quartzite assemblage extend eastward and interfinger with rocks of the graywacke-shale terrane. Rocks that are entirely of the graywacke-shale assemblage have been correlated in the present study. The stratified rocks west of the axis of the Green Mountain anticlinorium are of Cambrian(?), Cambrian, and Ordovician age; those to the east range in age from Cambrian to Devonian. The geotectonic setting of the region is the once mobile belt of the Appalachian orthogeosyncline, which is at the southeastern margin of the stable continental block, or craton, of North America. The orthogeosyncline was a belt, chiefly of subsidence, that embraced two parallel and adjoining longitudinal zones: the eugeosynclinal zone, which was more mobile, and the miogeosynclinal zone, which was less mobile. Second- and third-generation geosynclines are superimposed not only on the orthogeosyncline but also on adjoining parts of the craton. Uplift, and finally folding, gradually superseded subsidence in the orthogeosyncline. Local uplift, chiefly within the eugeosynclinal zone, provided most of the clastic sediments, principally those of the graywacke-shale assemblage. General stabilization of the western part of the orthogeosyncline at the end of the Ordovician was accompanied by eastward migration of the miogeosynclinal zone. Localized uplift within the eastern part of the orthogeosyncline at this time is marked by unconformities referred to the Taconic disturbance. Folding and uplift after the Early Devonian is shown by angular unconformities referred to the Acadian and Appalachian orogenies. The interpretation of the geotectonic relations of the bedded rocks is aided by critical features of the magmatic activity that began with, accompanied, and followed the diastrophism.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)71[531:SAGRIN]2.0.CO;2","usgsCitation":"Cady, W.M., 1960, Stratigraphic and geotectonic relationships in northern Vermont and southern Quebec: Economic Geology, v. 71, no. 5-6, p. 531-576, https://doi.org/10.1130/0016-7606(1960)71[531:SAGRIN]2.0.CO;2.","productDescription":"46 p.","startPage":"531","endPage":"576","costCenters":[],"links":[{"id":385800,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States, Canada","state":"Vermont, Quebec","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.5205078125,\n 43.37311218382002\n ],\n [\n -71.455078125,\n 43.37311218382002\n ],\n [\n -71.455078125,\n 45.98169518512228\n ],\n [\n -73.5205078125,\n 45.98169518512228\n ],\n [\n -73.5205078125,\n 43.37311218382002\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"5-6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Cady, W. M.","contributorId":64641,"corporation":false,"usgs":true,"family":"Cady","given":"W.","middleInitial":"M.","affiliations":[],"preferred":false,"id":816102,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220587,"text":"70220587 - 1960 - Occurrence of strontium in the surface and ground waters of Champaign county, Ohio","interactions":[],"lastModifiedDate":"2021-05-21T14:39:50.079798","indexId":"70220587","displayToPublicDate":"1960-01-01T13:30:04","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":"Occurrence of strontium in the surface and ground waters of Champaign county, Ohio","docAbstract":"Naturally occurring strontium was found in both surface and ground waters during an investigation of the water resources of Champaign County, Ohio. The strontium is related to the presence of celestite (strontium sulfate) in rocks associated with evaporite deposition. The principal source of celestite in Ohio is in rocks of Late Silurian age. Celestite is present also in the glacial deposits of western Ohio, which contain rock material of Late Silurian age. Total time in contact with the rock material seems to have a large effect upon concentrations of strontium in ground water. Streamflow, during low-flow periods, is made up largely of ground-water seepage and contains detectable strontium. Strontium has been found in ground water in other counties in western Ohio and in the brines of eastern Ohio.
","language":"English","publisherLocation":"Society of Economic Geologist","doi":"10.2113/gsecongeo.55.1.176","usgsCitation":"Feulner, A., and Hubble, J., 1960, Occurrence of strontium in the surface and ground waters of Champaign county, Ohio: Economic Geology, v. 55, no. 1, p. 176-186, https://doi.org/10.2113/gsecongeo.55.1.176.","productDescription":"11 p.","startPage":"176","endPage":"186","costCenters":[],"links":[{"id":385794,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Ohio","county":"Champaign County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -83.83186340332031,\n 40.063884174719156\n ],\n [\n -83.64303588867186,\n 40.063884174719156\n ],\n [\n -83.64303588867186,\n 40.16680597002458\n ],\n [\n -83.83186340332031,\n 40.16680597002458\n ],\n [\n -83.83186340332031,\n 40.063884174719156\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"55","issue":"1","noUsgsAuthors":false,"publicationDate":"1960-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Feulner, A.J.","contributorId":70796,"corporation":false,"usgs":true,"family":"Feulner","given":"A.J.","affiliations":[],"preferred":false,"id":816098,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hubble, J.H.","contributorId":99624,"corporation":false,"usgs":true,"family":"Hubble","given":"J.H.","email":"","affiliations":[],"preferred":false,"id":816099,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1094,"text":"1094 - 1960 - Geology and ground-water hydrology of the Redlands-Beaumont area, California, with special reference to ground-water outflow","interactions":[],"lastModifiedDate":"2024-09-03T21:05:26.158835","indexId":"1094","displayToPublicDate":"1960-01-01T12:39:48","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"title":"Geology and ground-water hydrology of the Redlands-Beaumont area, California, with special reference to ground-water outflow","docAbstract":"The Redlands-Beaumont area is bordered by the Santa Ana River on the north, the San Bernadina River on the northeast, the Yucaipa Hills and the San Gorgonio Pass on the east, and the Badlands and the San Jacinto fault on the south and south-west. Large alluvial fans underlie much of the area, but other landforms include alluvial benches, dissected alluvial hills, plains, terraces, and bedrock hills which locally protrude above the floors of the alluvial valleys.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/1094","collaboration":"Prepared in cooperation with the San Bernardino County Flood Control District.","usgsCitation":"Burnham, W., and Dutcher, L.C., 1960, Geology and ground-water hydrology of the Redlands-Beaumont area, California, with special reference to ground-water outflow, 352 p., https://doi.org/10.3133/1094.","productDescription":"352 p.","costCenters":[],"links":[{"id":433421,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/1094/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":289641,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/1094/report-thumb.jpg"}],"country":"United States","state":"California","city":"Beaumont, Redlands","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -117.2637864386227,\n 34.105233250065254\n ],\n [\n -117.2637864386227,\n 33.87256760375355\n ],\n [\n -116.9107764193285,\n 33.87256760375355\n ],\n [\n -116.9107764193285,\n 34.105233250065254\n ],\n [\n -117.2637864386227,\n 34.105233250065254\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53be6474e4b0527d5d4097b6","contributors":{"authors":[{"text":"Burnham, W.L.","contributorId":58668,"corporation":false,"usgs":true,"family":"Burnham","given":"W.L.","email":"","affiliations":[],"preferred":false,"id":143166,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dutcher, Lee Carlton","contributorId":32229,"corporation":false,"usgs":true,"family":"Dutcher","given":"Lee","email":"","middleInitial":"Carlton","affiliations":[],"preferred":false,"id":143165,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70160871,"text":"70160871 - 1960 - Geology and ground-water resources of the island of Kauai, Hawaii","interactions":[],"lastModifiedDate":"2016-01-06T08:58:28","indexId":"70160871","displayToPublicDate":"1960-01-01T12:15:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":242,"text":"Bulletin","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"13","title":"Geology and ground-water resources of the island of Kauai, Hawaii","docAbstract":"Kauai is one of the oldest, and is structurally the most complicated, of the Hawaiian Islands. Like the others, it consists principally of a huge shield volcano, built up from the sea floor by many thousands of thin flows of basaltic lava. The volume of the Kauai shield was on the order of 1,000 cubic miles. Through much of its growth it must have resembled rather closely the presently active shield volcano Mauna Loa, on the island of Hawaii. When the Kauai volcano started its growth is not known with certainty, but it is believed that activity started late in the Tertiary period, possibly in the early or middle part of the Pliocene epoch. Growth of the shield was rapid and probably was completed before the end of the Pliocene.
Toward the end of the growth of the shield, its summit collapsed to form a broad caldera, the largest that has been found in the Hawaiian Islands. Like the calderas of Kilauea and Mauna Loa, that of Kauai volcano had boundaries that were, in part, rather indefinite. The principal depression was bordered by less depressed fault blocks, some of which merged imperceptibly with the outer slopes of the volcano. Elsewhere the caldera rim was low, and flows spilled over it onto the outer slopes. The well-defined central depression of the Kauai caldera was approximately 10 to 12 miles across.
At about the same time as the formation of the major caldera, another, smaller caldera was formed by collapse around a minor eruptive center on the southeastern side of the Kauai shield. Lavas accumulated in the calderas, gradually filling them and burying banks of talus that formed along the foot of the boundary cliffs. The caldera-filling lavas differed from those that built the major portion of the shield in being much thicker and more massive as a result of ponding in the depressions. The petrographic types for the most part are the same throughout. Both the flank flows that built most of the shield and the flows that filled the calderas are predominantly olivine basalt. Picrite-basalt (oceanite), containing very abundant large phenocrysts of olivine, and basalt containing little or no olivine are present but together comprise less than 10 percent of the whole. Late in the period of filling of the major caldera a small amount of basaltic andesine andesite was extruded.
Near the end of the period of filling of the major caldera further collapse occurred, forming a large graben on the southwestern side of the shield. Lava flows erupting within the caldera poured southwestward over the cliff bounding the graben and spread over the gently sloping graben floor. Near the present Waimea Canyon their advance was obstructed by the fault scarp at the west edge of the graben. The cliff along the northeast edge of the graben eventually was buried by lava flows from within the caldera, but that along the west edge continued to stand above the level of the flows in the graben. The flows that accumulated in the graben are of the same types as those that filled the caldera, and like them are mostly thick and massive because of ponding by the graben walls and of the gentle slopes of the graben floor over which they spread.
The rocks of the major Kauai shield volcano are known as the Waimea Canyon volcanic series. The thin flows that accumulated on the flanks of the shield, which compose the major portion of the volcanic edifice, are named the Napali formation of the Waimea Canyon volcanic series. The rocks that accumulated in the big summit caldera are named the Olokele formation, and those that filled the small caldera on the southeast flank of the shield are named the Haupu formation. The volcanic rocks accumulated in the graben on the southwestern side of the shield are named the Makaweli formation of the Waimea Canyon volcanic series, and sedimentary rocks interbedded with them are known as the Mokuone member of the Makaweli formation.
Few vents of the Waimea Canyon volcanic series have been recognized, probably because most of them have been destroyed by erosion or are buried by later lavas. Large numbers of dikes cut the lavas of the Napali formation along Waimea Canyon and the Napali Coast and along the east edge of the Waialeale massif. Fewer dikes are found in the other members of the series. Some tendency toward radial arrangement of the dikes is present, but the dominant trend all over the island is east-northeastward.
Another great collapse took place on the eastern flank of the volcano at about the time the major shield became extinct, or shortly afterward. A subcircular graben 6 or 7 miles across sank several thousand feet, forming a broad depression between the Waialeale massif on the west and Kalepa and Nonou ridges on the east. This collapsed structure cannot be as clearly demonstrated as the Makaweli graben on the southwest side of the shield, because its walls have been greatly eroded and its floor is deeply buried by lavas of the later Koloa volcanic series. It appears, however, to be the only reasonable explanation of the physiography of the eastern side of the island.
After the completion of the great Kauai shield came a long period of erosion during which no volcanic activity occurred. Waves cut high sea cliffs around the island, and streams cut canyons as much as 3,000 feet deep. Thick soil formed over much of the mountain.
Then volcanism was renewed. Eruption occurred from a series of minor vents arranged in nearly north-south and northeast-southwest lines across the eastern two-thirds of the island. The lavas, cinder cones, and ash beds of this period of volcanism are known as the Koloa volcanic series. Lavas of the Koloa volcanic series include olivine basalt, picrite-basalt (mimosite) with few phenocrysts of olivine, basanite, nepheline basalt, melilite-nepheline basalt, and ankaratrite (nepheline basalt very rich in pyroxene and olivine). Inclusions of dunite, composed almost entirely of olivine, are common in flows of the Koloa. Just before and during the eruption of the Koloa volcanic series, voluminous landslides and mudflows brought down a large amount of rock debris and soil from the steep slopes of the mountainous central upland and deposited it as breccias at the foot of the steep slopes in valley heads and along the border of the marginal lowland. Streams distributed part of the material across the lowland. The breccias and conglomerates thus formed, and later buried by lavas of the Koloa volcanic series, are named the Palikea formation of the Koloa volcanic series.
The structures formed at Koloa vents include cinder cones, one tuff cone, and lava cones. The latter are miniature shields resembling the major shield volcano, formed by repeated outpourings of fluid lava. The tuff cone, at the west side of Kilauea Bay, was formed by phreatomagmatic explosions caused by rising magma coming in contact with water-saturated rocks.
Volcanism during Koloa time continued for a long period but was not continuous over the entire area. Locally, long periods of quiet occurred, allowing streams to re-excavate some of the canyons filled by earlier flows of the Koloa volcanic series, and weathering to form soils later buried by new flows. Some of the canyons thus formed during the time when the Koloa was being deposited were several hundred feet deep. Volcanism probably continued throughout most of the Pleistocene epoch. The latest flow of the Koloa volcanic series appears very recent, and rests on lithified calcareous dunes formed during one of the Pleistocene low stands of the sea.
During the Pleistocene epoch stream valleys and sea cliffs were eroded to base levels governed by one or more stands of the sea more than 100 feet below present sea level. Beaches of calcareous sand were formed, and the sand blown inland to form calcareous dunes, now lithified. A test boring near Moloaa penetrated calcareous sand 160 feet below sea level, at the foot of a high sea cliff. Coral reef also was built around part or all of the island, and in part buried by lavas of the Koloa volcanic series. The explosions that built the tuff cone at Kilauea Bay threw up fragments of limestone from a buried reef. Much of the apron of lavas of the Kalna series around the northeastern side of the island probably rests on a platform formed below present sea level by wave erosion and the growth of coral reef.
As the sea rose around the island, the valley mouths were alluviated. Several levels of the sea higher than the present one probably are represented. Some stream terraces may be graded to a stand of the sea as high as 260 feet above present sea level, but no positive evidence for stands higher than 25 feet have been found. Well-preserved shorelines are recognized approximately 25 and 5 feet above sea level. Much of the present coral reef appears to have been formed when the sea stood about 5 feet higher than now, and reduced to its present level by solutional weathering and wave erosion.
The lavas of the Napali formation of the Waimea Canyon volcanic series are highly permeable. They carry basal water over much of the island, and yield it freely to wells. This water is fresh everywhere except very close to the coast on the leeward side of the island. In some areas they may contain water confined at high levels between dikes. The lavas of the Olokele and Haupu formations are moderately to poorly permeable. They probably contain fresh water at sea level, but would not yield it readily to wells. Locally, ash beds perch small bodies of fresh water at high levels in the lavas of the Olokele formation, but these are of no economic importance. The lavas of the Makaweli formation also arc moderately to poorly permeable. They carry fresh or brackish water at sea level. In general, they yield water to wells less readily than the lavas of the Napali formation, but more readily than the lavas of the Olokele. The conglomerates and breccias of the Mokuone member are poorly permeable, but are not known to perch more than a slight amount of water in the overlying lavas,
The lava flows of the Koloa volcanic series are poorly to moderately permeable. They carry fresh or brackish water at sea level, but generally yield it slowly to wells. Locally, small bodies of fresh water are perched at high levels in the lavas of the Koloa by beds of ash and soil and by breccia and conglomerate of the Palikea formation.
Both the older and the younger alluvium generally are poorly permeable, but contain small amounts of fresh or brackish water. The lithified calcareous dunes are permeable, but they appear to contain only brackish water. Lagoon deposits on the Mana plain are poorly to moderately permeable and yield brackish water to wells.
The papers comprising the various parts of this report contain preliminary results of the U. S. Geological Survey investigations in the U12b.03 and U12b.04 tunnels at the Nevada Test Site, Nye County, Nevada (fig. 1). The geologic studies were undertaken to define the structural, chemical, mineralogic, and some of the physical properties of the tuffaceous rocks that enclose the explosion chambers at the end of each tunnel.
\nThe U12b.03 and .04 tunnels are part of the U12b (Rainier) tunnel complex that was driven northwestward from the steep east slope of Rainier Mesa (a prominent topographic feature in the northwest part of the Test Site (fig . 2)). The U12b.03 tunnel trends north from a point about 980 feet from the portal of the U12b tunnel (fig. 3). The U12b.03 tunnel consists of 620 feet of tunnel, two alcoves, and a shot chamber. The tunnel is irregular, ranging from 6 to 10 feet in width, and 6 to 9 feet in height. The shot chamber at the north end of the tunnel is 22 feet on each sidee The vertical and minimum cover over the shot chamber are 610 and 510 feet, respectively.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tem996","usgsCitation":"Diment, W., Wilmarth, V.R., McKeown, F.A., Dickey, D., Hinrichs, E., Botinelly, T., Roach, C.H., Byers, F., Hawley, C.C., Izett, G., and Clebsch, A., 1959, Geological investigations in the U12b.03 and U12b.04 tunnels, Nevada Test Site: U.S. Geological Survey Trace Elements Memorandum 996, Report: 73 p.; 4 Plates: 42.66 x 40.60 inches or smaller, https://doi.org/10.3133/tem996.","productDescription":"Report: 73 p.; 4 Plates: 42.66 x 40.60 inches or smaller","numberOfPages":"73","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":309873,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/tem996.jpg"},{"id":310387,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/0996/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}},{"id":310388,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":310389,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":310390,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":310391,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nevada","county":"Nye County","otherGeospatial":"Rainier Mesa","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-115.9082,39.1615],[-115.5191,38.9578],[-115.4725,38.9325],[-115.4433,38.9162],[-115.3694,38.8769],[-115.363,38.874],[-115.242,38.8093],[-115.0969,38.7309],[-115.0777,38.721],[-115.0604,38.7107],[-115.0291,38.6937],[-114.999,38.6777],[-114.9996,38.592],[-114.9997,38.4315],[-114.9994,38.3894],[-115.0004,38.0507],[-115.1185,38.0508],[-115.1436,38.0508],[-115.326,38.0515],[-115.3453,38.0514],[-115.4003,38.051],[-115.4587,38.0506],[-115.6394,38.0512],[-115.6581,38.051],[-115.8404,38.0504],[-115.8931,38.0507],[-115.8938,37.723],[-115.8969,37.5498],[-115.8975,37.2796],[-115.8982,37.1926],[-115.8942,36.8425],[-115.8941,36.686],[-115.8945,36.6702],[-115.8949,36.598],[-115.8949,36.5962],[-115.8946,36.5858],[-115.8947,36.5005],[-115.8945,36.4806],[-115.8949,36.462],[-115.8944,36.457],[-115.8948,36.3087],[-115.8945,36.2923],[-115.8943,36.1957],[-115.8945,36.1608],[-115.8948,36.1163],[-115.8948,36.0927],[-115.895,36.0015],[-115.9178,36.0192],[-115.9518,36.0457],[-115.9925,36.0773],[-116.049,36.1211],[-116.0624,36.1314],[-116.1039,36.1636],[-116.1287,36.1829],[-116.1702,36.2152],[-116.173,36.2174],[-116.2311,36.2626],[-116.2834,36.3028],[-116.2954,36.3122],[-116.3752,36.373],[-116.5107,36.4764],[-116.5247,36.4871],[-116.5589,36.5131],[-116.574,36.5245],[-116.5946,36.54],[-116.6556,36.5867],[-116.6583,36.5888],[-116.6764,36.6024],[-116.706,36.6248],[-116.7895,36.6877],[-116.8424,36.7276],[-116.8453,36.7298],[-116.8806,36.7568],[-116.8912,36.7648],[-116.9237,36.7891],[-116.9641,36.8193],[-116.9783,36.8299],[-116.981,36.8319],[-117.0046,36.8495],[-117.164,36.9688],[-117.1639,36.9698],[-117.1637,37.0182],[-117.164,37.0894],[-117.1642,37.171],[-117.1641,37.1909],[-117.1641,37.1936],[-117.1665,37.6995],[-117.1664,37.714],[-117.1663,37.7285],[-117.1663,37.7435],[-117.1662,37.7585],[-117.1657,38.0019],[-117.2198,38.0482],[-117.2397,38.0483],[-117.239,38.0641],[-117.2408,38.0705],[-117.2653,38.0932],[-117.6896,38.4731],[-118.0197,38.7599],[-118.197,38.9154],[-118.1972,38.9993],[-117.8559,39.0746],[-117.7748,39.092],[-117.7008,39.1058],[-117.6409,39.1149],[-117.5946,39.1231],[-117.4742,39.1431],[-117.3823,39.1562],[-117.3609,39.1585],[-117.3318,39.1629],[-117.3063,39.1634],[-117.2849,39.1633],[-117.1995,39.1632],[-117.0856,39.1628],[-117.0322,39.1626],[-117.0144,39.1626],[-116.9871,39.1625],[-116.9158,39.1631],[-116.7562,39.1622],[-116.7301,39.1625],[-116.5996,39.1616],[-116.5859,39.162],[-116.4815,39.1616],[-116.3497,39.1618],[-116.2358,39.1616],[-116.0548,39.1624],[-115.9082,39.1615]]]},\"properties\":{\"name\":\"Nye\",\"state\":\"NV\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"561f7cb5e4b03ee62faa8fe1","contributors":{"authors":[{"text":"Diment, W.H.","contributorId":54992,"corporation":false,"usgs":true,"family":"Diment","given":"W.H.","affiliations":[],"preferred":false,"id":577411,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilmarth, V. 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C.","contributorId":102070,"corporation":false,"usgs":true,"family":"Hawley","given":"C.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":577419,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Izett, G. A.","contributorId":21131,"corporation":false,"usgs":true,"family":"Izett","given":"G. A.","affiliations":[],"preferred":false,"id":577420,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Clebsch, Alfred","contributorId":57047,"corporation":false,"usgs":true,"family":"Clebsch","given":"Alfred","affiliations":[],"preferred":false,"id":577421,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":76909,"text":"tem1033 - 1959 - Thickness, character, and structure of upper Permian evaporites in part of Eddy County, New Mexico","interactions":[],"lastModifiedDate":"2015-11-02T13:42:37","indexId":"tem1033","displayToPublicDate":"2013-07-23T13:26:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":338,"text":"Trace Elements Memorandum","code":"TEM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1033","title":"Thickness, character, and structure of upper Permian evaporites in part of Eddy County, New Mexico","docAbstract":"Between Project Gnome site and the International Minerals and Chemical Corporation's plant site, in central eastern Eddy County, N. Mex., unconsolidated deposits of Quaternary age and redbeds of Triassic age attain a thickness of about 700 feet, and rest unconformably on evaporites of late Permian age. The upper Permian evaporites are 3,000 to 3,800 feet thick, and they are divided, in descending order, into the Rustler, Salado, and Castile formations. The Rustler is largely gypsum rock, the Salado is dominantly halite rock, and the Castile contains both anhydrite rock and halite rock. The salt and anhydrite beds of the Salado and Castile are intruded by narrow dikes of alkalic rock along which the evaporites are little altered. The sedimentary rocks have a generally southeastward regional dip, but locally are warped in gentle folds of low amplitude and fairly small lateral dimensions.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tem1033","collaboration":"Submitted to San Francisco Operations Office, U.S. Atomic Energy Commission.","usgsCitation":"Jones, C.L., 1959, Thickness, character, and structure of upper Permian evaporites in part of Eddy County, New Mexico: U.S. Geological Survey Trace Elements Memorandum 1033, Report: 19 p.; 2 Plates: 19.75 x 12.88 inches; Table, https://doi.org/10.3133/tem1033.","productDescription":"Report: 19 p.; 2 Plates: 19.75 x 12.88 inches; Table","numberOfPages":"21","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":290813,"rank":4,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/TEM1033.jpg"},{"id":310946,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/1033/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":310947,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/1033/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":310948,"rank":3,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/tem/1033/table-2.pdf","text":"Table 2","linkFileType":{"id":1,"text":"pdf"},"description":"Table 2"}],"country":"United States","state":"New Mexico","county":"Eddy County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-103.8111,32.9663],[-103.8112,32.903],[-103.8116,32.8876],[-103.8115,32.8725],[-103.8114,32.8575],[-103.8112,32.8429],[-103.8114,32.7974],[-103.8112,32.7823],[-103.8105,32.7122],[-103.8103,32.6971],[-103.8101,32.6247],[-103.81,32.6101],[-103.8097,32.5399],[-103.8096,32.5249],[-103.789,32.5245],[-103.7716,32.5246],[-103.7493,32.5242],[-103.7194,32.524],[-103.7166,32.524],[-103.7165,32.5085],[-103.7165,32.4916],[-103.7157,32.4429],[-103.7156,32.4278],[-103.7155,32.3535],[-103.7154,32.3385],[-103.7158,32.2692],[-103.7157,32.2546],[-103.7161,32.1817],[-103.716,32.1666],[-103.716,32.0918],[-103.7162,32.0631],[-103.7164,32.0015],[-103.9574,32.0011],[-103.9757,32.001],[-103.9936,32.001],[-104.0001,32.001],[-104.0011,32.001],[-104.0109,32.001],[-104.0265,32.001],[-104.0282,32.001],[-104.0617,32.0012],[-104.1475,32.0017],[-104.4014,32.0024],[-104.7313,32.0032],[-104.7467,32.0032],[-104.8299,32.0031],[-104.8466,32.0031],[-104.8464,32.0958],[-104.8462,32.1104],[-104.8463,32.1378],[-104.8461,32.1533],[-104.8457,32.2554],[-104.8495,32.2554],[-104.8493,32.3839],[-104.8496,32.399],[-104.8492,32.4286],[-104.8495,32.4427],[-104.8491,32.5124],[-104.849,32.5188],[-104.8392,32.5196],[-104.8389,32.5351],[-104.8384,32.608],[-104.8382,32.6253],[-104.8376,32.6986],[-104.8372,32.7268],[-104.8369,32.7856],[-104.8367,32.7992],[-104.8369,32.827],[-104.8366,32.8416],[-104.8364,32.8543],[-104.8362,32.8694],[-104.8357,32.903],[-104.8354,32.9659],[-104.8332,32.9659],[-104.8189,32.9662],[-104.8162,32.9661],[-104.802,32.966],[-104.7982,32.9659],[-104.779,32.9662],[-104.7686,32.9661],[-104.7621,32.966],[-104.7511,32.9664],[-104.7178,32.9664],[-104.7118,32.9664],[-104.7003,32.9662],[-104.6844,32.9661],[-104.6336,32.9664],[-104.6254,32.9663],[-104.6084,32.9665],[-104.5986,32.9664],[-104.3487,32.9663],[-104.3416,32.9661],[-104.3071,32.9661],[-104.2973,32.966],[-104.2896,32.9663],[-104.2803,32.9662],[-104.2617,32.9663],[-104.2552,32.9662],[-104.2448,32.9661],[-104.2382,32.9664],[-104.2278,32.9663],[-104.1939,32.9662],[-104.1758,32.9664],[-104.1589,32.9661],[-104.154,32.966],[-104.1425,32.9658],[-104.1365,32.9657],[-104.1327,32.9661],[-104.108,32.9662],[-104.1042,32.9661],[-104.0807,32.9662],[-104.0741,32.966],[-104.0643,32.9659],[-104.0523,32.9661],[-104.0495,32.9661],[-104.0402,32.9664],[-104.0348,32.9663],[-104.0315,32.9662],[-103.9834,32.9649],[-103.9741,32.9648],[-103.9593,32.965],[-103.9435,32.9651],[-103.9265,32.9653],[-103.8773,32.9657],[-103.8466,32.9661],[-103.8111,32.9663]]]},\"properties\":{\"name\":\"Eddy\",\"state\":\"NM\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"561e2b3be4b0cdb063e59cfa","contributors":{"authors":[{"text":"Jones, Charles Leslie","contributorId":27790,"corporation":false,"usgs":true,"family":"Jones","given":"Charles","email":"","middleInitial":"Leslie","affiliations":[],"preferred":false,"id":288141,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":71569,"text":"tei545 - 1959 - Gravity and seismic exploration in Yucca Valley, Nevada test site, January-April, 1959","interactions":[],"lastModifiedDate":"2015-10-20T13:04:38","indexId":"tei545","displayToPublicDate":"2013-07-18T11:22:00","publicationYear":"1959","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":"545","title":"Gravity and seismic exploration in Yucca Valley, Nevada test site, January-April, 1959","docAbstract":"The thickness of the alluvial and tuffaceous deposits that overlie bedrock in Yucca Valley has been inferred from gravity and seismic measurements. Preliminary interpretations indicate that these deposits are thickest in a narrow north-trending trough in the eastern part of the valley. The gravity data delineate a buried north-trending ridge of bedrock that extends from Mine Mountain almost to Quartzite Ridge.
\nSeismic refraction measurements confirm the existence of the bedrock ridge and indicate that the bedrock is as close as 100 feet to the surface. The buried bedrock high is important because it may alter concepts of the movement of groundwater within the valley.
\nA single seismic-refraction profile was located near the area of thickest alluvium and tuff to determine the feasibility of using refraction techniques for determining the depth to bedrock where it is covered with several thousand feet of alluvium and tuff. The results are encouraging but not enough data were acquired to give a reliable depth estimate.
\nSeismic-refraction measurements were used successfully to determine the thickness of alluvium in narrow valleys partly filled with alluvium.
\nThis work was in the northwestern part of Yucca Valley and was done to choose drilling sites for studies of ground-water movement.
\n","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/tei545","collaboration":"Work done on behalf of the Albuquerque Operations Office, U.S. Atomic Energy Commission.","usgsCitation":"Diment, W.H., Healey, D., and Roller, J., 1959, Gravity and seismic exploration in Yucca Valley, Nevada test site, January-April, 1959: U.S. Geological Survey Trace Elements Investigations 545, Report: 41 p.; 1 Plate: 21.26 x 34.69 inches, https://doi.org/10.3133/tei545.","productDescription":"Report: 41 p.; 1 Plate: 21.26 x 34.69 inches","numberOfPages":"44","onlineOnly":"N","additionalOnlineFiles":"Y","temporalStart":"1959-01-01","temporalEnd":"1959-04-30","costCenters":[],"links":[{"id":290451,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/tei545.jpg"},{"id":310154,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tei/545/report.pdf","text":"Report","size":"14.70 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":310155,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tei/545/plate-1.pdf","text":"Plate 1","size":"12.50 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"Nevada","county":"Nye County","otherGeospatial":"Yucca Valley","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-115.9082,39.1615],[-115.5191,38.9578],[-115.4725,38.9325],[-115.4433,38.9162],[-115.3694,38.8769],[-115.363,38.874],[-115.242,38.8093],[-115.0969,38.7309],[-115.0777,38.721],[-115.0604,38.7107],[-115.0291,38.6937],[-114.999,38.6777],[-114.9996,38.592],[-114.9997,38.4315],[-114.9994,38.3894],[-115.0004,38.0507],[-115.1185,38.0508],[-115.1436,38.0508],[-115.326,38.0515],[-115.3453,38.0514],[-115.4003,38.051],[-115.4587,38.0506],[-115.6394,38.0512],[-115.6581,38.051],[-115.8404,38.0504],[-115.8931,38.0507],[-115.8938,37.723],[-115.8969,37.5498],[-115.8975,37.2796],[-115.8982,37.1926],[-115.8942,36.8425],[-115.8941,36.686],[-115.8945,36.6702],[-115.8949,36.598],[-115.8949,36.5962],[-115.8946,36.5858],[-115.8947,36.5005],[-115.8945,36.4806],[-115.8949,36.462],[-115.8944,36.457],[-115.8948,36.3087],[-115.8945,36.2923],[-115.8943,36.1957],[-115.8945,36.1608],[-115.8948,36.1163],[-115.8948,36.0927],[-115.895,36.0015],[-115.9178,36.0192],[-115.9518,36.0457],[-115.9925,36.0773],[-116.049,36.1211],[-116.0624,36.1314],[-116.1039,36.1636],[-116.1287,36.1829],[-116.1702,36.2152],[-116.173,36.2174],[-116.2311,36.2626],[-116.2834,36.3028],[-116.2954,36.3122],[-116.3752,36.373],[-116.5107,36.4764],[-116.5247,36.4871],[-116.5589,36.5131],[-116.574,36.5245],[-116.5946,36.54],[-116.6556,36.5867],[-116.6583,36.5888],[-116.6764,36.6024],[-116.706,36.6248],[-116.7895,36.6877],[-116.8424,36.7276],[-116.8453,36.7298],[-116.8806,36.7568],[-116.8912,36.7648],[-116.9237,36.7891],[-116.9641,36.8193],[-116.9783,36.8299],[-116.981,36.8319],[-117.0046,36.8495],[-117.164,36.9688],[-117.1639,36.9698],[-117.1637,37.0182],[-117.164,37.0894],[-117.1642,37.171],[-117.1641,37.1909],[-117.1641,37.1936],[-117.1665,37.6995],[-117.1664,37.714],[-117.1663,37.7285],[-117.1663,37.7435],[-117.1662,37.7585],[-117.1657,38.0019],[-117.2198,38.0482],[-117.2397,38.0483],[-117.239,38.0641],[-117.2408,38.0705],[-117.2653,38.0932],[-117.6896,38.4731],[-118.0197,38.7599],[-118.197,38.9154],[-118.1972,38.9993],[-117.8559,39.0746],[-117.7748,39.092],[-117.7008,39.1058],[-117.6409,39.1149],[-117.5946,39.1231],[-117.4742,39.1431],[-117.3823,39.1562],[-117.3609,39.1585],[-117.3318,39.1629],[-117.3063,39.1634],[-117.2849,39.1633],[-117.1995,39.1632],[-117.0856,39.1628],[-117.0322,39.1626],[-117.0144,39.1626],[-116.9871,39.1625],[-116.9158,39.1631],[-116.7562,39.1622],[-116.7301,39.1625],[-116.5996,39.1616],[-116.5859,39.162],[-116.4815,39.1616],[-116.3497,39.1618],[-116.2358,39.1616],[-116.0548,39.1624],[-115.9082,39.1615]]]},\"properties\":{\"name\":\"Nye\",\"state\":\"NV\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd5f19e4b0b290850fc1de","contributors":{"authors":[{"text":"Diment, William H.","contributorId":78797,"corporation":false,"usgs":true,"family":"Diment","given":"William","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":284407,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Healey, D.L.","contributorId":52964,"corporation":false,"usgs":true,"family":"Healey","given":"D.L.","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":284406,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Roller, J. C.","contributorId":12507,"corporation":false,"usgs":true,"family":"Roller","given":"J.","middleInitial":"C.","affiliations":[],"preferred":false,"id":284405,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70047487,"text":"70047487 - 1959 - Ground-water resources of the Oakland Park area of eastern Broward County, Florida","interactions":[{"subject":{"id":24519,"text":"ofr5891 - 1958 - Ground-water resources of the Oakland Park area of eastern Broward County, Florida","indexId":"ofr5891","publicationYear":"1958","noYear":false,"title":"Ground-water resources of the Oakland Park area of eastern Broward County, Florida"},"predicate":"SUPERSEDED_BY","object":{"id":70047487,"text":"70047487 - 1959 - Ground-water resources of the Oakland Park area of eastern Broward County, Florida","indexId":"70047487","publicationYear":"1959","noYear":false,"title":"Ground-water resources of the Oakland Park area of eastern Broward County, Florida"},"id":1}],"lastModifiedDate":"2017-09-13T17:55:10","indexId":"70047487","displayToPublicDate":"2013-01-01T15:18:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5489,"text":"Florida Geological Survey Report of Investigations","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"20","title":"Ground-water resources of the Oakland Park area of eastern Broward County, Florida","docAbstract":"The Biscayne aquifer is the source of all fresh ground water in the Oakland Park area of eastern Broward County, Florida. This aquifer extends from the land surface to more than 215 feet below mean sea level and is composed chiefly of sandy marine limestone, calcareous sandstone, and beds of fine to medium quartz sand. The aquifer differs from place to place, but, in general, most of the layers of limestone and sandstone occur at depths below 60 feet. The permeability of the aquifer increases with depth.","language":"English","publisher":"Florida Geological Survey","publisherLocation":"Tallahassee, FL","collaboration":"Prepared by the United States Geological Survey in cooperation with the City of Fort Lauderdale and the Florida Geological Survey","usgsCitation":"Sherwood, C., 1959, Ground-water resources of the Oakland Park area of eastern Broward County, Florida: Florida Geological Survey Report of Investigations 20, vii, 40 p.","productDescription":"vii, 40 p.","costCenters":[],"links":[{"id":276179,"type":{"id":11,"text":"Document"},"url":"https://ufdc.ufl.edu/UF00001204/00001/pdf?search=report+%3dinvestigations"},{"id":276180,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70047487.PNG"}],"country":"United States","state":"Florida","county":"Broward County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -80.881389,25.95675 ], [ -80.881389,26.334667 ], [ -80.015276,26.334667 ], [ -80.015276,25.95675 ], [ -80.881389,25.95675 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5203a379e4b02bdb1bc63fa6","contributors":{"authors":[{"text":"Sherwood, C. B.","contributorId":27888,"corporation":false,"usgs":true,"family":"Sherwood","given":"C. B.","affiliations":[],"preferred":false,"id":482173,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5220549,"text":"5220549 - 1959 - Mourning dove management in Eastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:14:42","indexId":"5220549","displayToPublicDate":"2010-06-16T12:18:16","publicationYear":"1959","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3140,"text":"Proceedings of the Annual Conference of the Southeastern Association of Game and Fish Commissioners","active":true,"publicationSubtype":{"id":10}},"title":"Mourning dove management in Eastern United States","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Proceedings of the Annual Conference of the Southeastern Association of Game and Fish Commissioners","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","usgsCitation":"Kiel, W., 1959, Mourning dove management in Eastern United States: Proceedings of the Annual Conference of the Southeastern Association of Game and Fish Commissioners, v. 13, p. 19-21.","productDescription":"19-21","startPage":"19","endPage":"21","numberOfPages":"3","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":197039,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"13","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b47d3","contributors":{"authors":[{"text":"Kiel, W.H.","contributorId":105395,"corporation":false,"usgs":true,"family":"Kiel","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":331995,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":56161,"text":"ofr5976 - 1959 - Surface waters of Illinois River basin in Arkansas and Oklahoma","interactions":[],"lastModifiedDate":"2012-02-02T00:12:10","indexId":"ofr5976","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-76","title":"Surface waters of Illinois River basin in Arkansas and Oklahoma","docAbstract":"The estimated runoff from the Illinois River basin of 1,660 square miles has averaged 1,160,000 acre-feet per year during the water years 1938-56, equivalent to an average annual runoff depth of 13.1 inches. About 47 percent of the streamflow is contributed from drainage in Arkansas, where an average of 550,000 acre-ft per year runs off from 755 square miles, 45.5 percent of the total drainage area.\r\nThe streamflow is highly variable. Twenty-two years of record for Illinois River near Tahlequah, Okla., shows a variation in runoff for the water year 1945 in comparison with 1954 in a ratio of almost 10 to 1. Runoff in 1927 may have exceeded that of 1945, according to records for White River at Beaver, Ark., the drainage basin just east of the Illinois River basin. Variation in daily discharge is suggested by a frequency analysis of low flows at the gaging station near Tahlequah, Okla. The mean flow at that site is 901 cfs (cubic feet per second), the median daily flow is 350 cfs, and the lowest 30-day mean flow in a year probably will be less than 130 cfs half of the time and less than 20 cfs every 10 years on the average.\r\n\r\nThe higher runoff tends to occur in the spring months, March to May, a 3-month period that, on the average, accounts for almost half of the annual flow. High runoff may occur during any month in the year, but in general, the streamflow is the lowest in the summer. The mean monthly flow of Illinois River near Tahlequah, Okla., for September is about 11 percent of that for May. Records show that there is flow throughout the year in Illinois River and its principal tributaries Osage Creek, Flint Creek and Barren Fork.\r\n\r\nThe high variability in streamflow in this region requires the development of storage by impoundment if maximum utilization of the available water supplies is to be attained. For example, a 120-day average low flow of 22 cfs occurred in 1954 at Illinois River near Tahlequah, Okla. To have maintained the flow at 350 cfs, the median daily flow during the 19-year base period, an impoundment at that site would have required a usable storage of 185,000 acre-ft to satisfy this demand during the drought years 1954-1956.\r\n\r\nThe surface waters of the Illinois River basin are excellent quality being suitable for municipal, agriculture and most industrial uses. The average concentration of the dissolved mineral content is about 105 ppm (parts per million) and the hardness about 85 ppm. The water is slightly alkaline, having a range of pH values from 7.2 to 8.0.\r\n\r\nThis report gives the estimated average discharge at gaging stations and approximations of average discharge at the State line for 3 sub-basins during the 19-year period October 1937 to September 1956, used as a base period in this report. Duration-of-flow data for various percentages of the time are shown for the period of observed record at the gaging stations; similar data are estimated for the selected base period. Storage requirements to sustain flow during the recent drought years are given for 3 stations. The streamflow records in the basin are presented on a monthly and annual basis through September 1957; provisional records for 3 stations are included through July 1958 for correlation purposes. Results of discharge measurements are given for miscellaneous sites where low-flow observations have been made.\r\n\r\n(available as photostat copy only)","language":"ENGLISH","doi":"10.3133/ofr5976","usgsCitation":"Laine, L., 1959, Surface waters of Illinois River basin in Arkansas and Oklahoma: U.S. Geological Survey Open-File Report 59-76, 65 p., 13 figs., https://doi.org/10.3133/ofr5976.","productDescription":"65 p., 13 figs.","costCenters":[],"links":[{"id":184636,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aeee4b07f02db6912cd","contributors":{"authors":[{"text":"Laine, L.L.","contributorId":100464,"corporation":false,"usgs":true,"family":"Laine","given":"L.L.","email":"","affiliations":[],"preferred":false,"id":254854,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":72330,"text":"tem998 - 1959 - Geological Survey investigations in the U12b.01 tunnel, Nevada Test Site","interactions":[],"lastModifiedDate":"2015-11-02T13:58:00","indexId":"tem998","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":338,"text":"Trace Elements Memorandum","code":"TEM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"998","title":"Geological Survey investigations in the U12b.01 tunnel, Nevada Test Site","docAbstract":"
The U12b.01 tunnel is part of the U12b (Rainier) tunnel system driven northwestward from the east slope of Rainier Mesa (figs. 1 and 2). Geologic and geophysical studies in this tunnel were conducted by the U.S. Geological Survey on behalf of the Albuquerque Operations Office of the Atomic Energy Commission. This report includes a brief description of the stratigraphy and structure, and data on petrology, mineralogy, and chemical and physical properties of the rocks that are exposed in the tunnel.
\nThe U12b.01 tunnel trends N. 10° W., and connects with the Ul2b tunnel at about 500 feet from the portal (fig. 2). The U12b,01 tunnel is about 250 feet long and contains an alcove 40 feet long and 20 feet wide, and a shot chamber 17 by 20 feet. The tunnel is irregular and ranges from 6 to 15 feet in width and averages 7 feet in height. Much of the tunnel has been supported using 6-foot steel sets and wood planks for lagging Vertical and minimum cover over the shot chamber at west end of the tunnel are approximately the same, about 295 feet.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tem998","usgsCitation":"Diment, W.H., Wilmarth, V., McKeown, F.A., Dickey, D., Botinelly, T., Hinrichs, E., Roach, C.H., Byers, F., Izett, G., and Johnson, G., 1959, Geological Survey investigations in the U12b.01 tunnel, Nevada Test Site: U.S. Geological Survey Trace Elements Memorandum 998, Report: 39 p.; 2 Plates: 17.73 x 20.57 inches and 15.06 x 19.09 inches, https://doi.org/10.3133/tem998.","productDescription":"Report: 39 p.; 2 Plates: 17.73 x 20.57 inches and 15.06 x 19.09 inches","numberOfPages":"39","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":310952,"rank":301,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0998/plate-4.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 4"},{"id":91096,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/0998/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":191562,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/tem/0998/report-thumb.jpg"},{"id":310953,"rank":302,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0998/plate-6.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 6"}],"country":"United States","state":"Nevada","county":"Nye County","otherGeospatial":"Rainier Mesa","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-115.9082,39.1615],[-115.5191,38.9578],[-115.4725,38.9325],[-115.4433,38.9162],[-115.3694,38.8769],[-115.363,38.874],[-115.242,38.8093],[-115.0969,38.7309],[-115.0777,38.721],[-115.0604,38.7107],[-115.0291,38.6937],[-114.999,38.6777],[-114.9996,38.592],[-114.9997,38.4315],[-114.9994,38.3894],[-115.0004,38.0507],[-115.1185,38.0508],[-115.1436,38.0508],[-115.326,38.0515],[-115.3453,38.0514],[-115.4003,38.051],[-115.4587,38.0506],[-115.6394,38.0512],[-115.6581,38.051],[-115.8404,38.0504],[-115.8931,38.0507],[-115.8938,37.723],[-115.8969,37.5498],[-115.8975,37.2796],[-115.8982,37.1926],[-115.8942,36.8425],[-115.8941,36.686],[-115.8945,36.6702],[-115.8949,36.598],[-115.8949,36.5962],[-115.8946,36.5858],[-115.8947,36.5005],[-115.8945,36.4806],[-115.8949,36.462],[-115.8944,36.457],[-115.8948,36.3087],[-115.8945,36.2923],[-115.8943,36.1957],[-115.8945,36.1608],[-115.8948,36.1163],[-115.8948,36.0927],[-115.895,36.0015],[-115.9178,36.0192],[-115.9518,36.0457],[-115.9925,36.0773],[-116.049,36.1211],[-116.0624,36.1314],[-116.1039,36.1636],[-116.1287,36.1829],[-116.1702,36.2152],[-116.173,36.2174],[-116.2311,36.2626],[-116.2834,36.3028],[-116.2954,36.3122],[-116.3752,36.373],[-116.5107,36.4764],[-116.5247,36.4871],[-116.5589,36.5131],[-116.574,36.5245],[-116.5946,36.54],[-116.6556,36.5867],[-116.6583,36.5888],[-116.6764,36.6024],[-116.706,36.6248],[-116.7895,36.6877],[-116.8424,36.7276],[-116.8453,36.7298],[-116.8806,36.7568],[-116.8912,36.7648],[-116.9237,36.7891],[-116.9641,36.8193],[-116.9783,36.8299],[-116.981,36.8319],[-117.0046,36.8495],[-117.164,36.9688],[-117.1639,36.9698],[-117.1637,37.0182],[-117.164,37.0894],[-117.1642,37.171],[-117.1641,37.1909],[-117.1641,37.1936],[-117.1665,37.6995],[-117.1664,37.714],[-117.1663,37.7285],[-117.1663,37.7435],[-117.1662,37.7585],[-117.1657,38.0019],[-117.2198,38.0482],[-117.2397,38.0483],[-117.239,38.0641],[-117.2408,38.0705],[-117.2653,38.0932],[-117.6896,38.4731],[-118.0197,38.7599],[-118.197,38.9154],[-118.1972,38.9993],[-117.8559,39.0746],[-117.7748,39.092],[-117.7008,39.1058],[-117.6409,39.1149],[-117.5946,39.1231],[-117.4742,39.1431],[-117.3823,39.1562],[-117.3609,39.1585],[-117.3318,39.1629],[-117.3063,39.1634],[-117.2849,39.1633],[-117.1995,39.1632],[-117.0856,39.1628],[-117.0322,39.1626],[-117.0144,39.1626],[-116.9871,39.1625],[-116.9158,39.1631],[-116.7562,39.1622],[-116.7301,39.1625],[-116.5996,39.1616],[-116.5859,39.162],[-116.4815,39.1616],[-116.3497,39.1618],[-116.2358,39.1616],[-116.0548,39.1624],[-115.9082,39.1615]]]},\"properties\":{\"name\":\"Nye\",\"state\":\"NV\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db688031","contributors":{"authors":[{"text":"Diment, William H.","contributorId":78797,"corporation":false,"usgs":true,"family":"Diment","given":"William","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":285443,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilmarth, V.R.","contributorId":20803,"corporation":false,"usgs":true,"family":"Wilmarth","given":"V.R.","email":"","affiliations":[],"preferred":false,"id":285440,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McKeown, F. A.","contributorId":106100,"corporation":false,"usgs":true,"family":"McKeown","given":"F.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":285446,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Dickey, D.D.","contributorId":15612,"corporation":false,"usgs":true,"family":"Dickey","given":"D.D.","email":"","affiliations":[],"preferred":false,"id":285438,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Botinelly, T.","contributorId":20408,"corporation":false,"usgs":true,"family":"Botinelly","given":"T.","affiliations":[],"preferred":false,"id":285439,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Hinrichs, E. N.","contributorId":98717,"corporation":false,"usgs":true,"family":"Hinrichs","given":"E. N.","affiliations":[],"preferred":false,"id":285445,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Roach, C. H.","contributorId":12117,"corporation":false,"usgs":true,"family":"Roach","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":285437,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Byers, F. M.","contributorId":50141,"corporation":false,"usgs":true,"family":"Byers","given":"F. M.","affiliations":[],"preferred":false,"id":285442,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Izett, G. A.","contributorId":21131,"corporation":false,"usgs":true,"family":"Izett","given":"G. A.","affiliations":[],"preferred":false,"id":285441,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Johnson, G. R.","contributorId":90290,"corporation":false,"usgs":true,"family":"Johnson","given":"G. R.","affiliations":[],"preferred":false,"id":285444,"contributorType":{"id":1,"text":"Authors"},"rank":10}]}} ,{"id":64315,"text":"gp205 - 1959 - Aeromagnetic map of the East Greenville quadrangle, Berks, Lehigh, and Montgomery Counties, Pennsylvania","interactions":[],"lastModifiedDate":"2021-12-06T22:24:35.22011","indexId":"gp205","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"205","title":"Aeromagnetic map of the East Greenville quadrangle, Berks, Lehigh, and Montgomery Counties, Pennsylvania","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp205","usgsCitation":"Bromery, R.W., and Zandle, G.L., 1959, Aeromagnetic map of the East Greenville quadrangle, Berks, Lehigh, and Montgomery Counties, Pennsylvania: U.S. Geological Survey Geophysical Investigations Map 205, 1 Plate: 22.90 × 26.96 inches, https://doi.org/10.3133/gp205.","productDescription":"1 Plate: 22.90 × 26.96 inches","costCenters":[],"links":[{"id":392532,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_3124.htm"},{"id":251708,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0205/report-thumb.jpg"},{"id":250953,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0205/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":250952,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0205/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"Pennsylvania","county":"Berks County, Lehigh County, Montgomery County","otherGeospatial":"East Greenville quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.625,40.375 ], [ -75.625,40.5 ], [ -75.5,40.5 ], [ -75.5,40.375 ], [ -75.625,40.375 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6974fd","contributors":{"authors":[{"text":"Bromery, Randolph Wilson","contributorId":22746,"corporation":false,"usgs":true,"family":"Bromery","given":"Randolph","email":"","middleInitial":"Wilson","affiliations":[],"preferred":false,"id":270542,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zandle, G. L.","contributorId":39863,"corporation":false,"usgs":true,"family":"Zandle","given":"G.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":270543,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":47166,"text":"ofr5915 - 1959 - Geologic map of the Curlew quadrangle, Ferry County, Washington","interactions":[{"subject":{"id":47166,"text":"ofr5915 - 1959 - Geologic map of the Curlew quadrangle, Ferry County, Washington","indexId":"ofr5915","publicationYear":"1959","noYear":false,"title":"Geologic map of the Curlew quadrangle, Ferry County, Washington"},"predicate":"SUPERSEDED_BY","object":{"id":35444,"text":"b1169 - 1964 - Geology of the Curlew quadrangle, Ferry County, Washington","indexId":"b1169","publicationYear":"1964","noYear":false,"title":"Geology of the Curlew quadrangle, Ferry County, Washington"},"id":1}],"supersededBy":{"id":35444,"text":"b1169 - 1964 - Geology of the Curlew quadrangle, Ferry County, Washington","indexId":"b1169","publicationYear":"1964","noYear":false,"title":"Geology of the Curlew quadrangle, Ferry County, Washington"},"lastModifiedDate":"2023-08-11T16:01:46.480413","indexId":"ofr5915","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-15","title":"Geologic map of the Curlew quadrangle, Ferry County, Washington","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5915","usgsCitation":"Calkins, J.A., Parker, R., and Disbrow, A.E., 1959, Geologic map of the Curlew quadrangle, Ferry County, Washington: U.S. Geological Survey Open-File Report 59-15, 2 Plates: 17.49 x 26.40 inches and 19.08 x 24.43 inches, https://doi.org/10.3133/ofr5915.","productDescription":"2 Plates: 17.49 x 26.40 inches and 19.08 x 24.43 inches","costCenters":[],"links":[{"id":135764,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":106299,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_7952.htm","linkFileType":{"id":5,"text":"html"},"description":"7952"}],"country":"United States","state":"Washington","county":"Ferry County","otherGeospatial":"Curlew quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.5,\n 49\n ],\n [\n -118.75,\n 49\n ],\n [\n -118.75,\n 48.75\n ],\n [\n -118.5,\n 48.75\n ],\n [\n -118.5,\n 49\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b09e4b07f02db69bd89","contributors":{"authors":[{"text":"Calkins, James Alfred","contributorId":75504,"corporation":false,"usgs":true,"family":"Calkins","given":"James","email":"","middleInitial":"Alfred","affiliations":[],"preferred":false,"id":234738,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Parker, R. L.","contributorId":19170,"corporation":false,"usgs":true,"family":"Parker","given":"R. L.","affiliations":[],"preferred":false,"id":880092,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Disbrow, Alan Eastman","contributorId":83895,"corporation":false,"usgs":true,"family":"Disbrow","given":"Alan","email":"","middleInitial":"Eastman","affiliations":[],"preferred":false,"id":234739,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":61435,"text":"mf182 - 1959 - Bedrock geology of the northern and eastern parts of the North Range, Cuyuna district, Minnesota","interactions":[],"lastModifiedDate":"2019-05-28T08:25:02","indexId":"mf182","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"182","title":"Bedrock geology of the northern and eastern parts of the North Range, Cuyuna district, Minnesota","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/mf182","usgsCitation":"Schmidt, R.G., 1959, Bedrock geology of the northern and eastern parts of the North Range, Cuyuna district, Minnesota: U.S. Geological Survey Miscellaneous Field Studies Map 182, 1 map on 5 sheets, https://doi.org/10.3133/mf182.","productDescription":"1 map on 5 sheets","costCenters":[],"links":[{"id":182872,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/0182/report-thumb.jpg"},{"id":364160,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364161,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364159,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364163,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364162,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"7200","country":"United States","state":"Minnesota","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -94.1,46.45 ], [ -94.1,46.55 ], [ -93.81694444444445,46.55 ], [ -93.81694444444445,46.45 ], [ -94.1,46.45 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5ee4b07f02db633f4b","contributors":{"authors":[{"text":"Schmidt, R. G.","contributorId":107690,"corporation":false,"usgs":true,"family":"Schmidt","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":265637,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":61459,"text":"mf210 - 1959 - Preliminary geologic and structure map of the east-central part of the Cascade Springs quadrangle, Fall River County, South Dakota","interactions":[],"lastModifiedDate":"2018-12-14T11:15:19","indexId":"mf210","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"210","title":"Preliminary geologic and structure map of the east-central part of the Cascade Springs quadrangle, Fall River County, South Dakota","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf210","usgsCitation":"Post, E., and Lane, D.W., 1959, Preliminary geologic and structure map of the east-central part of the Cascade Springs quadrangle, Fall River County, South Dakota: U.S. Geological Survey Miscellaneous Field Studies Map 210, 36.46 x 31.65 inches, https://doi.org/10.3133/mf210.","productDescription":"36.46 x 31.65 inches","costCenters":[],"links":[{"id":182681,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/0210/report-thumb.jpg"},{"id":360306,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0210/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","county":"Fall River County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -130.5,43.284166666666664 ], [ -130.5,43.333333333333336 ], [ -103.55111111111111,43.333333333333336 ], [ -103.55111111111111,43.284166666666664 ], [ -130.5,43.284166666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699b77","contributors":{"authors":[{"text":"Post, Edwin V.","contributorId":80330,"corporation":false,"usgs":true,"family":"Post","given":"Edwin V.","affiliations":[],"preferred":false,"id":265690,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lane, Donald W.","contributorId":15511,"corporation":false,"usgs":true,"family":"Lane","given":"Donald","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":265691,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":47377,"text":"b1082C - 1959 - Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","interactions":[{"subject":{"id":13430,"text":"ofr5473 - 1954 - Iron deposits of North America, Cuba, and Puerto Rico","indexId":"ofr5473","publicationYear":"1954","noYear":false,"title":"Iron deposits of North America, Cuba, and Puerto Rico"},"predicate":"SUPERSEDED_BY","object":{"id":47377,"text":"b1082C - 1959 - Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","indexId":"b1082C","publicationYear":"1959","noYear":false,"chapter":"C","title":"Iron-ore resources of the United States including Alaska and Puerto Rico, 1955"},"id":1},{"subject":{"id":47377,"text":"b1082C - 1959 - Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","indexId":"b1082C","publicationYear":"1959","noYear":false,"chapter":"C","title":"Iron-ore resources of the United States including Alaska and Puerto Rico, 1955"},"predicate":"IS_PART_OF","object":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"id":2}],"isPartOf":{"id":33208,"text":"b1082 - 1962 - Contributions to economic geology, 1958","indexId":"b1082","publicationYear":"1962","noYear":false,"title":"Contributions to economic geology, 1958"},"lastModifiedDate":"2024-09-24T18:21:40.983129","indexId":"b1082C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"C","title":"Iron-ore resources of the United States including Alaska and Puerto Rico, 1955","docAbstract":"The importance of iron ore, the basic raw material of steel, as a fundamental mineral, resource is shown by the fact that about 100 million long tons of steel is used annually in the economy of the United States, as compared with a combined total of about 5 million long tons of copper, lead, zinc, and aluminum. Satisfying this annual demand for steel requires about 110 million tons of iron ore and 70 million tons of scrap iron and steel.
The average annual consumption of iron ore in the United States from 1951 to 1955, inclusive, was about 110 million long tons, which is about twice the annual average from 1900 to 1930. Production of iron ore in the United States in this 5-year period averaged approximately 100 million long tons annually, divided by regions as follows (in percent): Lake Superior, 84.1; southeastern, 6.7; western, 6.7; northeastern, 1.4; and central and gulf, 1.1.
Mining of iron ore began in the American Colonies about 1619, and for 225 years it was limited to eastern United States where fuel and markets were readily available. Production of iron ore from the Lake Superior region began in 1846; the region became the leading domestic source by 1890, and the Mesabi range in Minnesota has been the world's most productive area since 1896. Proximity of raw materials, water transportation, and markets has resulted in centralization of the country's iron and steel industry in the lower Great Lakes area. Increased imports of iron ore being delivered to eastern United States as well as demands for steel in nearby markets have given impetus to expansion in the steel-making capacity in this area.
The four chief iron-ore minerals - hematite, liminite, magnetite, and siderite - are widely distributed but only locally form deposits of sufficient tonnage and grade to be commercially valuable at the present time. The iron content of these minerals, of which hematite is the most important, ranges from 48 percent in siderite to 72 percent in magnetite, but as these minerals are associated with other rock-forming minerals, the iron content of marketable ore has a lower range from 30 to 67 percent.
Chemical constituents other than iron also are important in determining the marketability of iron ore. Although some iron ores can be used in the blast furnace as mined, others must first be improved either chemically by reduction of undesirable constituents, or physically by aggregation. Phosphorus and sulfur particularly are common deleterious elements; excessive silica is also undesirable but within certain limits can be controlled by additional flux. Lime and magnesia are beneficial in specified amounts because of their fluxing qualities, and a small amount of alumina improves the fluidity of slag. Manganese is especially desirable as a deoxidizing and desulfurizing agent. Titanium, chromium, and nickel must also be considered in the use of ore containing these elements.
The principal iron-ore deposits in the United States have been formed by three processes. Hematite-bearing bedded deposits such as those at Birmingham, Ala., are marine sedimentary rocks which, except for weathering along the outcrop, have remained practically unaltered since deposition. Deposits of the Lake Superior region, also in sedimentary strata, originally had a slightly lower iron content than those at-Birmingham, but ore bodies of hematite and limonite were formed by removal of other constituents in solution after deposition of the beds, with a relative increase of iron content in the material remaining. Limestone adjacent to igneous intrusions has been replaced by magnetite deposits at Cornwall, Pa., and by hematite-magnetite deposits near Cedar City, Utah. Magnetite deposits in New Jersey and in the Adirondack Mountains of New York are generally believed to have been formed by replacement of grains of other minerals in metamorphic rocks.
Iron-ore resources are made up of reserves of iron ore, material usable under existing economic and technologic conditions; and potential ore, material likely to become usable under more favorable conditions. The tonnage and grade of material of combined reserves and potential ore in each of the deposits known or believed to contain at least 200,000 long tons of iron-ore resources are tabulated in this report, and numerous sources of additional information are given in a selected bibliography.
The total domestic iron-ore resources are estimated at approximately 75,000 million long tons of crude ore. About 10,000 million tons of the resources is reserves of crude ore that will probably yield 5,500 million tons of concentrates and direct-shipping ore. About 65,000 million tons is potential ore and may yield 25,000 million tons of concentrates and some direct-shipping ore.
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","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/om195","usgsCitation":"Durham, D., and Yerkes, R.F., 1959, Geologic map of the eastern Puente Hills, Los Angeles basin, California: U.S. Geological Survey Oil and Gas Investigation Map 195, Plate: 58.85 x 42.08 inches, https://doi.org/10.3133/om195.","productDescription":"Plate: 58.85 x 42.08 inches","costCenters":[],"links":[{"id":187524,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":104976,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_5348.htm","linkFileType":{"id":5,"text":"html"},"description":"5348"}],"scale":"24000","country":"United States ","state":"California ","otherGeospatial":"Puente Hills, Los Angeles basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.8750,\n 33.8750\n ],\n [\n -117.6250,\n 33.8750\n ],\n [\n -117.6250,\n 34.00\n ],\n [\n -117.8750,\n 34.00\n ],\n [\n -117.8750,\n 33.8750\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688b0d","contributors":{"authors":[{"text":"Durham, D.L.","contributorId":62257,"corporation":false,"usgs":true,"family":"Durham","given":"D.L.","email":"","affiliations":[],"preferred":false,"id":279342,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Yerkes, R. F.","contributorId":24754,"corporation":false,"usgs":true,"family":"Yerkes","given":"R.","middleInitial":"F.","affiliations":[],"preferred":false,"id":279341,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":12993,"text":"ofr5918 - 1959 - Steatitization of serpentinite bodies in north-central Vermont","interactions":[{"subject":{"id":12993,"text":"ofr5918 - 1959 - Steatitization of serpentinite bodies in north-central Vermont","indexId":"ofr5918","publicationYear":"1959","noYear":false,"title":"Steatitization of serpentinite bodies in north-central Vermont"},"predicate":"SUPERSEDED_BY","object":{"id":33900,"text":"b1122B - 1963 - Bedrock Geology and Asbestos Deposits of the Upper Missisquoi Valley and Vicinity, Vermont","indexId":"b1122B","publicationYear":"1963","noYear":false,"chapter":"B","title":"Bedrock Geology and Asbestos Deposits of the Upper Missisquoi Valley and Vicinity, Vermont"},"id":1}],"supersededBy":{"id":33900,"text":"b1122B - 1963 - Bedrock Geology and Asbestos Deposits of the Upper Missisquoi Valley and Vicinity, Vermont","indexId":"b1122B","publicationYear":"1963","noYear":false,"title":"Bedrock Geology and Asbestos Deposits of the Upper Missisquoi Valley and Vicinity, Vermont"},"lastModifiedDate":"2025-06-02T13:59:02.921516","indexId":"ofr5918","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-18","title":"Steatitization of serpentinite bodies in north-central Vermont","docAbstract":"The talc deposits of north-central Vermont are associated with bodies of ultramafic rock, chiefly serpentinite, that are enclosed by metamorphosed sedimentary and volcanic rocks of Cambrian and Ordovician age; these stratified rocks form an essentially homoclinal succession in the east limb of the Green Mountain anticlinorium. The rocks at the localities described here are in the greenschist facies, and show only slight variations in grade of metamorphism between localities.
The talc deposits consist typically of a core of serpentinite surrounded by successive shells of talc-carbonate rock and of steatite, next to which the country rock is altered for several inches to chlorite rock (blackwall). The steatite zone is rather uniformly about 3 feet thick, but the talc-carbonate rock and serpentinite zones vary considerably in thickness and are locally very irregular.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr5918","usgsCitation":"Chidester, A., 1959, Steatitization of serpentinite bodies in north-central Vermont: U.S. Geological Survey Open-File Report 59-18, Report: v, 69 p.; 2 Tables: 10.74 x 11.62 inches and 10.79 x 13.51 inches; 5 Figures: 10.48 x 15.89 inches or smaller, https://doi.org/10.3133/ofr5918.","productDescription":"Report: v, 69 p.; 2 Tables: 10.74 x 11.62 inches and 10.79 x 13.51 inches; 5 Figures: 10.48 x 15.89 inches or smaller","costCenters":[],"links":[{"id":489354,"rank":9,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1959/0018/Figure-5.pdf","text":"Figure 5","linkFileType":{"id":1,"text":"pdf"}},{"id":489353,"rank":8,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/of/1959/0018/Figure-4.pdf","text":"Figure 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