{"pageNumber":"348","pageRowStart":"8675","pageSize":"25","recordCount":11004,"records":[{"id":70014047,"text":"70014047 - 1984 - A review of crust and upper mantle structure studies of the Snake River Plain-Yellowstone volcanic system: A major lithospheric anomaly in the western U.S.A.","interactions":[],"lastModifiedDate":"2025-08-26T16:52:03.221469","indexId":"70014047","displayToPublicDate":"2003-04-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"A review of crust and upper mantle structure studies of the Snake River Plain-Yellowstone volcanic system: A major lithospheric anomaly in the western U.S.A.","docAbstract":"<p>The Snake River Plain-Yellowstone volcanic system is one of the largest, basaltic, volcanic field in the world. Here, there is clear evidence for northeasterly progression of rhyolitic volcanism with its present position in Yellowstone. Many theories have been advanced for the origin of the Snake River Plain-Yellowstone system. Yellowstone and Eastern Snake River Plain have been studied intensively using various geophysical techniques. Some sparse geophysical data are available for the Western Snake River Plain as well. Teleseismic data show the presence of a large anomalous body with low P- and S-wave velocities in the crust and upper mantle under the Yellowstone caldera. A similar body in which compressional wave velocity is lower than in the surrounding rock is present under the Eastern Snake River Plain. No data on upper mantle anomalies are available for the Western Snake River Plain. Detailed seismic refraction data for the Eastern Snake River Plain show strong lateral heterogeneities and suggest thinning of the granitic crust from below by mafic intrusion. Available data for the Western Snake River Plain also show similar thinning of the upper crust and its replacement by mafic material. The seismic refraction results in Yellowstone show no evidence of the low-velocity anomalies in the lower crust suggested by teleseismic P-delay data and interpreted as due to extensive partial melting. However, the seismic refraction models indicate lower-than-normal velocities and strong lateral inhomogeneities in the upper crust. Particularly obvious in the refraction data are two regions of very low seismic velocities near the Mallard Eake and Sour Creek resurgent domes in the Yellowstone caldera. The low-velocity body near the Sour Creek resurgent dome is interpreted as partially molten rock. Together with other geophysical and thermal data, the seismic results indicate that a sub-lithospheric thermal anomaly is responsible for the time-progressive volcanism along the Eastern Snake River Plain. However, the exact mechanism responsible for the volcanism and details of magma storage and migration are not yet fully understood.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(84)90209-9","issn":"00401951","usgsCitation":"Iyer, H.M., 1984, A review of crust and upper mantle structure studies of the Snake River Plain-Yellowstone volcanic system: A major lithospheric anomaly in the western U.S.A.: Tectonophysics, v. 105, no. 1-4, p. 291-308, https://doi.org/10.1016/0040-1951(84)90209-9.","productDescription":"18 p.","startPage":"291","endPage":"308","costCenters":[],"links":[{"id":226198,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Idaho, Montana, Nevada, Oregon, Washington, Wyoming","otherGeospatial":"Snake River Plain","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -120.75522630969246,\n              48.99647522967908\n            ],\n            [\n              -121.34357181116266,\n              40.94856106036778\n            ],\n            [\n              -120.51316857399542,\n              40.82964955876772\n            ],\n            [\n              -116.84272791453125,\n              41.89549551259576\n            ],\n            [\n              -115.64848818410448,\n              41.3864499907779\n            ],\n            [\n              -113.86318033209798,\n              41.953660184765866\n            ],\n            [\n              -110.16687892122758,\n              43.55396021584184\n            ],\n            [\n              -110.88285627702768,\n              48.99647522967908\n            ],\n            [\n              -120.75522630969246,\n              48.99647522967908\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"105","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e54fe4b0c8380cd46c9a","contributors":{"authors":[{"text":"Iyer, H. M.","contributorId":17997,"corporation":false,"usgs":true,"family":"Iyer","given":"H.","middleInitial":"M.","affiliations":[],"preferred":false,"id":367448,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70013436,"text":"70013436 - 1984 - Transport and concentration controls for chloride, strontium, potassium and lead in Uvas Creek, a small cobble-bed stream in Santa Clara County, California, U.S.A.: 1. Conceptual model","interactions":[],"lastModifiedDate":"2025-04-15T16:08:38.668793","indexId":"70013436","displayToPublicDate":"2003-03-27T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2342,"text":"Journal of Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"Transport and concentration controls for chloride, strontium, potassium and lead in Uvas Creek, a small cobble-bed stream in Santa Clara County, California, U.S.A.: 1. Conceptual model","docAbstract":"<p><span>Stream sediments adsorb certain solutes from streams, thereby significantly changing the solute composition; but little is known about the details and rates of these adsorptive processes. To investigate such processes, a 24-hr. injection of a solution containing chloride, strontium, potassium, sodium and lead was made at the head of a 640-m reach of Uvas Creek in west-central Santa Clara County, California. Uvas Creek is a cobble-bed pool-and-riffle stream draining the eastern slopes of the Santa Cruz Mountains. By September 12, 1973, after a long dry season, Uvas Creek had a low (0.0215 m</span><sup>3</sup><span>s</span><sup>−1</sup><span>&nbsp;average) flow which varied diurnally, from 0.018 to 0.025 m</span><sup>3</sup><span>s</span><sup>−1</sup><span>. Because stream discharge varied while the injection rate was constant, the concentration of tracers (injected solutes), after mixing in the stream, varied inversely with discharge.</span></p><p><span>Chloride, a nonreactive solute, served as a tracer of water movement. Analysis of extensive chloride concentration data at five sites below the injection point during and after the injection demonstrated that there was considerable underflow of water through the stream gravels; however, the extent of underflow varied greatly within the study reach. Pre-injection water, displaced by tracer-laden water percolating through the gravels, diluted tracers in the stream channel, giving the mistaken impression of groundwater inflow at some points. Accurate measurement of total discharge in such streams requires prolonged tracer injection unless a reach can be found where underflow is negligible.</span></p><p><span>Strontium and potassium were adsorbed by the bed sediments to a moderate extent and lead was strongly adsorbed. A high proportion of these metals could be removed by adsorption from percolating underflow because of extensive and intimate contact with bed sediments. After channel clearing following injection cutoff, 51% of the added strontium and 96% of the lead remained in the study reach, whereas only 19% of the chloride remained. Packets of sized sediment, placed in the stream before the experiment and withdrawn during and after the injection, indicated that the strontium absorbed on the 0.42–0.50-mm size sediment appeared to achieve near equilibrium with dissolved strontium within less than 2 hr. whereas 3.4–4.0-mm grains had not reached that stage after 24 hr.</span></p><p><span>The cation-exchange capacity (CEC) of the sediments shows a “bimodal” distribution with grain size. Largest values are in the finest sizes, lower values in the fine-to-medium sand-size range, intermediate values in the coarse- to very coarse-grained sand, and decreasing values with size above very coarse-grained sand. This considerable exchange capacity in coarse-sand to granule-size particles means that a streambed, that has not been infilled with fines to reduce permeability, can be highly reactive and accessible throughout a rather thick sediment layer and hence have a large and available reactive capacity.</span></p><p><span>As stream discharge increases from low flow, the ratio of underflow to channel flow should decrease rapidly with resultant diminution in percent of solutes sorbed within a particular stream reach.</span></p>","language":"English","publisher":"Elsevier","doi":"10.1016/0022-1694(84)90046-5","issn":"00221694","usgsCitation":"Kennedy, V.C., Jackman, A.P., Zand, S., Zellweger, G.W., and Avanzino, R., 1984, Transport and concentration controls for chloride, strontium, potassium and lead in Uvas Creek, a small cobble-bed stream in Santa Clara County, California, U.S.A.: 1. Conceptual model: Journal of Hydrology, v. 75, no. 1-4, p. 67-110, https://doi.org/10.1016/0022-1694(84)90046-5.","productDescription":"44 p.","startPage":"67","endPage":"110","costCenters":[],"links":[{"id":220588,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","county":"Santa Clara County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"id\":227,\"properties\":{\"name\":\"Santa 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W.","contributorId":55445,"corporation":false,"usgs":true,"family":"Zellweger","given":"G.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":366061,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Avanzino, R.J.","contributorId":37336,"corporation":false,"usgs":true,"family":"Avanzino","given":"R.J.","affiliations":[],"preferred":false,"id":366058,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70013401,"text":"70013401 - 1984 - Use of a digital model to evaluate hydrogeologic controls on groundwater flow in a fractured rock aquifer at Niagara Falls, New York, U.S.A.","interactions":[],"lastModifiedDate":"2025-04-15T15:51:34.651381","indexId":"70013401","displayToPublicDate":"2003-03-27T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2342,"text":"Journal of Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"Use of a digital model to evaluate hydrogeologic controls on groundwater flow in a fractured rock aquifer at Niagara Falls, New York, U.S.A.","docAbstract":"<p>The Hyde Park landfill is a 15-acre (6.1 ha) chemical waste disposal site located north of Niagara Falls, New York. Underlying the site in descending order are: (1) low-permeability glacial till and lacustrine deposits; (2) a moderately permeable fractured rock aquifer - the Lockport Dolomite; and (3) a low-permeability unit - the Rochester Shale. The site is bounded on three sides by groundwater drains; the Niagara River gorge, the Niagara Power Project canal, and the Niagara Power Project buried conduits. </p><p>The mechanism by which groundwater moves through fractured rocks underlying a hazardous waste site was investigated using a digital simulation approach. Three hypotheses were tested related to flow in the fractured rocks underlying Hyde Park landfill. For this purpose we used a Galerkin finite-element approximation to solve a saturated-unsaturated flow equation. </p><p><span>A primary focus was to investigate anisotropy in the Lockport Dolomite, that is the effectiveness of horizontal (bedding) joints vs. vertical joints as water-transmitting openings. Three hydrogeologic scenarios were set up — each with prescribed limits on the hydrologic parameters. Scenario&nbsp;</span><i>1</i><span>&nbsp;specified strongly anisotropic conditions in the Lockport Dolomite (horizontal hydraulic conductivity along bedding joints exceeds vertical conductivity by 2–3 orders of magnitude), uniform areal recharge (5 in. yr.</span><sup>−1</sup><span>&nbsp;or 12.7 cm yr.</span><sup>−1</sup><span>) except at the landfill where there is no recharge, and no flow through the base of the Rochester Shale. Scenario&nbsp;</span><i>2</i><span>&nbsp;also specified strongly anisotropic conditions in the Lockport; however, areal recharge was 6 in. yr.</span><sup>−1</sup><span>&nbsp;(15.2 cm yr.</span><sup>−1</sup><span>) except at the landfill where the recharge was 2 in. yr.</span><sup>−1</sup><span>&nbsp;(5.1 cm yr.</span><sup>−1</sup><span>), and outflow from the Rochester occurred. Scenario&nbsp;</span><i>3</i><span>&nbsp;specified isotropic conditions (that is, permeability along horizontal and vertical joints is the same in the Lockport Dolomite), recharge rates were the same as in scenario&nbsp;</span><i>2</i><span>&nbsp;and outflow through Rochester occurred.</span></p><p>Scenario 2 provided the closest agreement between the simulated and measured heads while scenario 3 provided the poorest agreement. Among the three scenarios tested, scenario 2 (with strongly anisotropic conditions in the Lockport Dolomite with added recharge through the landfill cap and limited flow through the Rocherster Shale) is considered the most realistic hydrogeologic model. </p><p>Based on simulation with the hydrogeologic parameters of scenario 2, groundwater flow near the Hyde Park site can be summarized as follows: </p><p>1. (1) <span>Specific discharge (Darcy velocity) ranges from ≈0.01 to 0.1 ft. day</span><sup>−1</sup><span>&nbsp;(0.003 to 0.03 m day</span><sup>−1</sup><span>) in the upper unit of the Lockport Dolomite to slightly more than 0.0001 ft. day</span><sup>−1</sup><span>&nbsp;(0.00003 m day</span><sup>−1</sup><span>) in the Rochester Shale. Real velocities are highest in the upper unit of the Lockport, ranging from ≈1 to 5 ft. day</span><sup>−1</sup><span>&nbsp;(0.3 to 1.5 m day</span><sup>−1</sup><span>) if the average effective porosity is assumed to be 0.02.</span></p><p>2. (2) A groundwater divide exists east of the landfill, indicating that all groundwater originating near or flowing beneath the landfill will flow toward and discharge in the gorge. </p><p>3. (3) Highest flow velocities (and presumably greatest potential for transporting chemical contaminants) occur in the upper unit of the Lockport and part of the lower unit of the Lockport Dolomite between the landfill and the gorge. The average time required for groundwater to move from the landfill to the discharge points at the gorge along selected flow paths in the Lockport Dolomite is estimated to be 5-6 yr.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0022-1694(84)90049-0","issn":"00221694","usgsCitation":"Maslia, M., and Johnston, R., 1984, Use of a digital model to evaluate hydrogeologic controls on groundwater flow in a fractured rock aquifer at Niagara Falls, New York, U.S.A.: Journal of Hydrology, v. 75, no. 1-4, p. 167-194, https://doi.org/10.1016/0022-1694(84)90049-0.","productDescription":"28 p.","startPage":"167","endPage":"194","costCenters":[],"links":[{"id":220091,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York","otherGeospatial":"Niagara Falls","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -79.07144327825095,\n              43.09286795115449\n            ],\n            [\n              -79.07144327825095,\n              43.07801889165893\n            ],\n            [\n              -79.05037086913583,\n              43.07801889165893\n            ],\n            [\n              -79.05037086913583,\n              43.09286795115449\n            ],\n            [\n              -79.07144327825095,\n              43.09286795115449\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","volume":"75","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bbe8fe4b08c986b329661","contributors":{"authors":[{"text":"Maslia, M.L.","contributorId":24090,"corporation":false,"usgs":true,"family":"Maslia","given":"M.L.","affiliations":[],"preferred":false,"id":365990,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnston, R.H.","contributorId":19536,"corporation":false,"usgs":true,"family":"Johnston","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":365989,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":60252,"text":"mf1246L - 1984 - Maps showing distribution of pH, copper, zinc, fluoride, uranium, molybdenum, arsenic, and sulfate in water, Richfield 1° x 2° quadrangle, Utah","interactions":[],"lastModifiedDate":"2021-10-25T19:02:48.751765","indexId":"mf1246L","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1984","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":"1246","chapter":"L","title":"Maps showing distribution of pH, copper, zinc, fluoride, uranium, molybdenum, arsenic, and sulfate in water, Richfield 1° x 2° quadrangle, Utah","docAbstract":"<p>These maps show the regional distribution of copper, zinc, arsenic, molybdenum, uranium, fluoride, sulfate, and pH in surface and ground water from the Richfield 1° x 2° quadrangle. This study supplements (Miller and others, 1984a-j) the regional drainage geochemical study done for the Richfield quadrangle under the U.S. Geological Survey’s Conterminuous United States Mineral Assessment Program (CUSMAP). Regional sampling was designed to define broad geochemical patterns and trends which can be used, along with geologic and geophysical data, to assess the mineral resource potential of the Richfield quadrangle. Analytical data used in compiling this report were published previously (McHugh and others, 1981).</p>\n<br/>\n<p>The Richfield quadrangle in west-central Utah covers the eastern part of the Pioche-Marysvale igneous and mineral belt that extends from the vicinity of Pioche in southeastern Nevada, east-northeastward for 250 km into central Utah. The western two-thirds of the Richfield quadrangle is in the Basin and Range Province, and the eastern third in the High Plateaus of Utah subprovince of the Colorado Plateau.</p>\n<br/>\n<p>Bedrock in the northern part of the Richfield quadrangle consists predominantly of latest Precambrian and Paleozoic sedimentary strata that were thrust eastward during the Sevier orogeny in Cretaceous time onto an autochthon of Mesozoic sedimentary rocks in the eastern part of the quadrangle. The southern part of the quadrangle is largely underlain by Oligocene and younger volcanic rocks and related intrusions. Extensional tectonism in late Cenozoic time broke the bedrock terrane into a series of north-trending fault blocks; the uplifted mountain areas were deeply eroded and the resulting debris deposited in the adjacent basins. Most of the mineral deposits in the Pioche-Marysvale mineral belt were formed during igneous activity in the middle and late Cenozoic time.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver CO","doi":"10.3133/mf1246L","usgsCitation":"McHugh, J.B., Miller, W.R., and Ficklin, W.H., 1984, Maps showing distribution of pH, copper, zinc, fluoride, uranium, molybdenum, arsenic, and sulfate in water, Richfield 1° x 2° quadrangle, Utah: U.S. Geological Survey Miscellaneous Field Studies Map 1246, 1 Plate: 40.89 x 32.77 inches, https://doi.org/10.3133/mf1246L.","productDescription":"1 Plate: 40.89 x 32.77 inches","costCenters":[],"links":[{"id":182629,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1246l.jpg"},{"id":283659,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1246-L/plate-1.pdf"},{"id":390899,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_6856.htm"}],"scale":"500000","country":"United States","state":"Utah","otherGeospatial":"Richfield 1° x 2° quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -114.0,38.0 ], [ -114.0,39.0 ], [ -112.0,39.0 ], [ -112.0,38.0 ], [ -114.0,38.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a19e4b07f02db60578b","contributors":{"authors":[{"text":"McHugh, J. B.","contributorId":79462,"corporation":false,"usgs":true,"family":"McHugh","given":"J.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":263391,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, W. R.","contributorId":92239,"corporation":false,"usgs":true,"family":"Miller","given":"W.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":263393,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ficklin, W. H.","contributorId":89517,"corporation":false,"usgs":true,"family":"Ficklin","given":"W.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":263392,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":38585,"text":"pp1278 - 1984 - The thrust belt in Southwest Montana and east-central Idaho","interactions":[],"lastModifiedDate":"2013-12-13T13:33:32","indexId":"pp1278","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1278","title":"The thrust belt in Southwest Montana and east-central Idaho","docAbstract":"The leading edge of the Cordilleran fold and thrust in southwest Montana appears to be a continuation of the edge of the Wyoming thrust belt, projected northward beneath the Snake River Plain. Trces of the thrust faults that form the leading edge of the thrust belts are mostly concealed, but stratigraphic and structural evidence suggests that the belt enters Montana near the middle of the Centennial Mountains, continues west along the Red Rock River valley, and swings north into the Highland Mountains near Butte. The thrust belt in southwest Montana and east-central Idaho includes at least two major plates -- the Medicine Lodge and Grasshopper thrust plates -- each of which contains a distinctive sequence of rocks, different in facies and structural style from those of the cratonic region east of the thrust belt. The thrust plates are characterized by persuasive, open to tight and locally overturned folds, and imbricate thrust faults, structural styles unusual in Phanerozoic cratonic rocks. The basal decollement zones of the plates are composed of intensely sheared, crushed, brecciated, and mylonitized rocks, the decollement at the base of the Medicine Lodge plate is as much as 300 meters thick. The Medicine Lodge and Grasshopper thrust plates are fringed on the east by a 10- to 50-kilometer-wide zone of tightly folded rocks cut by imbricate thrust fauls, a zone that forms the eastern margin of the thrust belt in southwest Montana. The frontal fold and thrust zone includes rocks that are similar to those of the craton, even though they differ in details of thickness, composition, or stratigraphic sequence. The zone is interpreted to be one of terminal folding and thrusting in cratonic rocks overridden by the major thrust plates from farther west. The cratonic rocks were drape-folded over rising basement blocks that formed a foreland bulge in front of the thrust belt. The basement blocks are bounded by steep faults of Proterozoic ancestry, which also moved as tear faults during thrusting, and seem to have controlled the curving patterns of salients and reentrants at the leading edge of the thrust belt. Radiometric and stratiographic evidence shows that the thrust belt was in its present position by about 75 million year go.","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp1278","usgsCitation":"Ruppel, E., and Lopez, D.A., 1984, The thrust belt in Southwest Montana and east-central Idaho: U.S. Geological Survey Professional Paper 1278, Report: iii, 41 p.; 1 Plate: 27.32 x 21.52 inches, https://doi.org/10.3133/pp1278.","productDescription":"Report: iii, 41 p.; 1 Plate: 27.32 x 21.52 inches","numberOfPages":"45","costCenters":[],"links":[{"id":170194,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1278/report-thumb.jpg"},{"id":279485,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1278/plate-1.pdf"},{"id":279486,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1278/report.pdf"}],"country":"United States","state":"Idaho;Montana","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -114.0,43.0 ], [ -114.0,46.0 ], [ -111.0,46.0 ], [ -111.0,43.0 ], [ -114.0,43.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db634a5f","contributors":{"authors":[{"text":"Ruppel, Edward T.","contributorId":7609,"corporation":false,"usgs":true,"family":"Ruppel","given":"Edward T.","affiliations":[],"preferred":false,"id":220112,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lopez, David A.","contributorId":79445,"corporation":false,"usgs":true,"family":"Lopez","given":"David","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":220113,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":9617,"text":"ofr84867 - 1984 - Assessment of ground-water contamination by coal-tar derivatives, St. Louis Park area, Minnesota","interactions":[],"lastModifiedDate":"2018-03-12T12:06:21","indexId":"ofr84867","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-867","title":"Assessment of ground-water contamination by coal-tar derivatives, St. Louis Park area, Minnesota","docAbstract":"<p>Operation of a coal-tar distillation and wood-preserving facility in St. Louis Park, Minnesota, during 1918-72 contaminated ground water with coal-tar derivatives and inorganic chemicals. Coal-tar derivatives entered the groundwater system through three major paths: (1) Spills and drippings that percolated to the water table, (2) surface runoff and plant process water that was discharged to wetlands south of the former plant site, and (3) movement of coal tar directly into bedrock aquifers through a multiaquifer well on the site.</p>\n<p>In the drift, Platteville, and St. Peter aquifers, ground water flows laterally from west to east and vertically downward. Near the former plant site, creosote-like organic fluids have migrated vertically downward through the drift and are being partially dissolved by ground water. Ground water has preferentially mobilized low-molecular-weight compounds such as phenolic compounds, alkyl-benzenes, and naphthalene, although polynuclear aromatic hydrocarbons as heavy as benzo(a)pyrene have been mobilized at low concentrations. Sorption of high-molecular-weight compounds has retarded their migration down the hydraulic gradient compared to low-molecular-weight compounds in the plume. Some simple phenolic compounds are being degraded to methane and carbon dioxide by bacteria under anaerobic conditions in the drift-PlattevilleSt. Peter aquifer system. Other low-molecular-weight aromatic compounds are apparently being degraded by aerobic bacteria at the periphery of the plume where oxygen is available. Intermediate degradation products such as volatile fatty acids are likely present, but complete conversion of the organic contaminants to innocuous inorganic substances has not been demonstrated. Near and south of 36th and Wooddale Avenues, contaminants enter the St. Peter aquifer where the Glenwood confining unit has been eroded in a buried bedrock valley. Contaminants previously entered the Prairie du Chien-Jordan aquifer through at least one multiaquif er well (W38). Other sources of contaminants and the low concentrations of contaminants hamper delineation of the maximum areal extent of contaminants that are resistant to biologic degradation. These biorefractory compounds will probably continue to migrate down the hydraulic gradients in the drift and Platteville and St. Peter aquifers.</p>\n<p>Of particular concern with respect to the health risk to humans are the polynuclear aromatic hydrocarbons, which are a major constituent of coal tar and are found in municipal wells near the site that are completed in the Prairie du Chien-Jordan aquifer. The Prairie du Chien-Jordan aquifer lies 250 to 500 feet below land surface and is relatively well protected from nearsurface sources of contamination by overlying rocks. However, the aquifer has been contaminated since at least 1932 because coal-tar derivatives have entered the aquifer through multiaquifer wells. The most significant single source of contamination in the aquifer is a well drilled on the site in 1917 (well W23) that has contained liquid coal-tar since at least 1958. The introduction, dissolution, and movement of this coal-tar in ground water has contaminated nearby municipal wells. The composition of the tar in well W23, and the ratio of concentrations of individual compounds in water from well W23 to those in municipal well SLP15, are consistent with known hydrologic, chemical, and biologic processes, and the conclusion that contaminants in well SLP15 are due primarily to contaminants introduced at well W23. Most of the major polynuclear aromatic hydrocarbons in the tar, although slightly soluble in water and strongly sorbed by aquifer materials, have moved greater distances at higher concentrations than have the lower-molecular-weight, more soluble compounds such as phenolic compounds and naphthalene. The latter are apparently being degraded by bacteria.</p>\n<p>The direction and rate of contaminant movement within the Prairie du Chien-Jordan aquifer changes with time because the ground-water-flow system continually adjusts to hydraulic stresses caused by ground-water withdrawals and flow through multiaquifer wells. Contaminants can move rapidly through the Prairie du Chien-Jordan because the upper part of the aquifer is a carbonate rock having fracture and solution-channel permeability, low effective porosity, and relatively small surface area for sorption. Consequently, the concentration and composition of contaminants in water pumped from individual industrial and municipal wells completed in the aquifer fluctuate with time. Although contaminants have been in the aquifer for at least 50 years and their spatial distribution is complex, concentrations remain highest near their points of introduction through multiaquifer wells near and on the site of the former plant.</p>\n<p>Contaminants reached the Ironton-Galesville aquifer through at least two deep multiaquifer wells (W23 and W38), but the extent of contamination in this aquifer, and in the underlying Mount Simon-Hinckley aquifer, is not known.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"St. Paul, MN","doi":"10.3133/ofr84867","collaboration":"Prepared in cooperation with the Minnesota Department of Health, Minnesota Pollution Control Agency, City of St. Louis Park, and the U.S. Environmental Protection Agency","usgsCitation":"Hult, M.F., 1984, Assessment of ground-water contamination by coal-tar derivatives, St. Louis Park area, Minnesota: U.S. Geological Survey Open-File Report 84-867, v, 57 p., https://doi.org/10.3133/ofr84867.","productDescription":"v, 57 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":37343,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0867/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":141739,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0867/report-thumb.jpg"}],"country":"United States","state":"Minnesota","city":"St. Louis Park","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -93.40164184570312,\n              44.918382411519346\n            ],\n            [\n              -93.40164184570312,\n              44.966012492248325\n            ],\n            [\n              -93.3024215698242,\n              44.966012492248325\n            ],\n            [\n              -93.3024215698242,\n              44.918382411519346\n            ],\n            [\n              -93.40164184570312,\n              44.918382411519346\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4abae4b07f02db671fa2","contributors":{"authors":[{"text":"Hult, M. F.","contributorId":29817,"corporation":false,"usgs":true,"family":"Hult","given":"M.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":160002,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":38532,"text":"pp1312 - 1984 - The Richmond and Greenwich slices of the Hamburg klippe in eastern Pennsylvania — Stratigraphy, sedimentology, structure, and plate tectonic implications","interactions":[],"lastModifiedDate":"2022-09-12T21:48:12.293122","indexId":"pp1312","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1312","title":"The Richmond and Greenwich slices of the Hamburg klippe in eastern Pennsylvania — Stratigraphy, sedimentology, structure, and plate tectonic implications","docAbstract":"<p>No abstract available.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1312","usgsCitation":"Lash, G.G., and Drake, A.A., 1984, The Richmond and Greenwich slices of the Hamburg klippe in eastern Pennsylvania — Stratigraphy, sedimentology, structure, and plate tectonic implications: U.S. Geological Survey Professional Paper 1312, 40 p., https://doi.org/10.3133/pp1312.","productDescription":"40 p.","costCenters":[],"links":[{"id":406568,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_74325.htm","linkFileType":{"id":5,"text":"html"}},{"id":65295,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1312/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122276,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1312/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"Richmond and Greenwich slices of the Hamburg klippe","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -76.0519,\n              40.4614\n            ],\n            [\n              -75.6978,\n              40.4614\n            ],\n            [\n              -75.6978,\n              40.6889\n            ],\n            [\n              -76.0519,\n              40.6889\n            ],\n            [\n              -76.0519,\n              40.4614\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac7e4b07f02db67acbe","contributors":{"authors":[{"text":"Lash, G. G.","contributorId":60648,"corporation":false,"usgs":true,"family":"Lash","given":"G.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":220010,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Drake, Avery A. Jr.","contributorId":81090,"corporation":false,"usgs":true,"family":"Drake","given":"Avery","suffix":"Jr.","middleInitial":"A.","affiliations":[],"preferred":false,"id":220011,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":30297,"text":"wri844180 - 1984 - Quality of water in the alluvial aquifer, American Bottoms, East St. Louis, Illinois","interactions":[],"lastModifiedDate":"2022-02-07T21:25:16.629118","indexId":"wri844180","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"84-4180","title":"Quality of water in the alluvial aquifer, American Bottoms, East St. Louis, Illinois","docAbstract":"<p>Ground-water levels in the American Bottoms regions around East St. Louis, Illinois, have risen several feet since the early 1970's. Artificial dewatering of the aquifer by increased pumping is being investigated by the U.S. Army Corps of Engineers to alleviate economic and health concerns resulting from elevated ground-water levels. A ground-water quality evaluation is necessary for selecting a feasible dewatering scheme. Analyses of water samples from 63 wells show that except for iron, manganese, and dissolved solids, constituent concentrations do not exceed Illinois water-quality standards. The waters are primarily of the calcium-magnesium-bicarbonate type with some calcium-sulfate type water. Iron concentrations ranged from less than 3 to 82,000 micrograms per liter, manganese from 5 to 5,300 micrograms per liter, and dissolved solids from 140 to 3,000 milligrams per liter. These constituent concentrations exceed Illinois ' public water supply, effluent, and general water-quality standards in most samples and analysis indicates the concentrations are representative of the ambient water quality. Concentrations of nitrite + nitrate nitrogen fluoride, zinc, lead, and sulfate also exceeded Illinois water-quality standards in a few samples. Concentrations of organic pesticides, polychlorinated biphenyls, and polychlorinated naphthalenes were below analytical detection limits.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri844180","usgsCitation":"Voelker, D.C., 1984, Quality of water in the alluvial aquifer, American Bottoms, East St. Louis, Illinois: U.S. Geological Survey Water-Resources Investigations Report 84-4180, v, 51 p., https://doi.org/10.3133/wri844180.","productDescription":"v, 51 p.","costCenters":[],"links":[{"id":395572,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_36048.htm"},{"id":159756,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1984/4180/report-thumb.jpg"},{"id":59086,"rank":299,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1984/4180/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Illinois","city":"East St. Louis","otherGeospatial":"American Bottoms","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -90.283,\n              38.5\n            ],\n            [\n              -89.967,\n              38.5\n            ],\n            [\n              -89.967,\n              38.917\n            ],\n            [\n              -90.283,\n              38.917\n            ],\n            [\n              -90.283,\n              38.5\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a8be4b07f02db6515f7","contributors":{"authors":[{"text":"Voelker, David C. dvoelker@usgs.gov","contributorId":278,"corporation":false,"usgs":true,"family":"Voelker","given":"David","email":"dvoelker@usgs.gov","middleInitial":"C.","affiliations":[{"id":346,"text":"Indiana Water Science Center","active":true,"usgs":true}],"preferred":true,"id":203009,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":59768,"text":"mf1713 - 1984 - Types of damage that could result from a great earthquake in the New Madrid, Missouri, seismic zone","interactions":[],"lastModifiedDate":"2026-02-23T21:30:35.522784","indexId":"mf1713","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"1713","title":"Types of damage that could result from a great earthquake in the New Madrid, Missouri, seismic zone","docAbstract":"<p>In the winter of 1811&ndash;1812 a series of three great earthquakes occurred in the New Madrid seismic zone. In addition to the three principal shocks, at least 15 other earthquakes, I<sub>o</sub> &ge; VIII, occurred within a year of the first large earthquake on December 16, 1811. The three main shocks were felt over the entire eastern United States. They were strong enough to cause minor damage as far away as Indiana and Ohio on the north, the Carolinas on the east, and southern Mississippi on the south. They were strong enough to cause severe or structural damage in parts of Missouri, Illinois, Indiana, Kentucky, Tennessee, Mississippi, and Arkansas. The section of this poster titled \"Seismic history of the New Madrid region\" describes what happened in the epicentral region. Fortunately, few people lived in the severely shaken area in 1811; that is not the case today. What would happen if a series of earthquakes as large and numerous as the \"New Madrid\" earthquakes were to occur in the New Madrid seismic zone today?</p>\n<p>Photographs 1-10 show typical damage to structures that occurred during various earthquakes in the United States. Structural damage to buildings in the Modified Mercalli intensity scale, a scale used for assigning numbers to earthquake effects, begins at intensity VIII. Minor or architectural damage (cracked plaster, windows, and chimneys) occurs at intensities VI and VII, and effects on people and small objects predominate at intensities below VI (earthquake felt, direction and duration noted, dishes broken). Photographs 1-10 illustrate damage caused by intensity VIII and above. None of the damage shown in these photographs occurred in earthquakes larger than the 1811&ndash;1812 New Madrid shocks, and most of the examples are from considerably smaller shocks. Photographs 1-4 and 7 show damage to masonry buildings, mostly old and unreinforced, none designed to be earthquake resistant. How many such buildings are in use in your community? Photographs 5 and 6 show damage to modern structures close to the epicenter of a magnitude 6.5 earthquake, a small shock compared to the magnitudes (8.4&ndash;8.7) of the New Madrid earthquakes. Photographs 8&ndash;10 are typical of damage that can occur at large distances from great earthquakes. Tall buildings are particularly susceptible to ground motions with relatively long periods (greater than 1 second), while short, rigid buildings are generally more likely to be damaged by ground motions with periods of less than 1 second. Shorter period ground motions attenuate more rapidly with distance from the epicenter than do the longer period motions.</p>\n<p>The 1811-1812 earthquakes produced extensive ground effects. Earthquakes can cause many different kinds of ground effects, ranging from minor fissures, slumps, and rockslides to major landslides and disturbances of the ground surface. Photographs 1117 show typical earthquake ground effects and the kinds of damage they can cause to manmade structures.</p>\n<p>Is another earthquake as large as the 1811-1812 shocks really likely to occur in New Madrid seismic zone? Great earthquakes such as the 1811-1812 series are estimated to occur in the zone on the average every 500 years. However, earthquakes strong enough to cause structural damage (VIII in the Modified Mercalli intensity scale) are estimated to occur in the seismic zone on the average every 50 years. The last such shock occurred in 1843.</p>\n<p>How do you prepare for a possible earthquake and what do you do if one occurs? The section on \"Earthquake safety tips\" explains what to do before, during, and after an earthquake.</p>\n<p>Want to know more? See \"Sources of additional information.\" Other reports of interest are listed in \"References cited.\"</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/mf1713","collaboration":"Prepared in cooperation with the Federal Emergency Management Agency","usgsCitation":"Hopper, M.G., and Algermissen, S.T., 1984, Types of damage that could result from a great earthquake in the New Madrid, Missouri, seismic zone: U.S. Geological Survey Miscellaneous Field Studies Map 1713, Plate: 42.18 x 28.92 inches, https://doi.org/10.3133/mf1713.","productDescription":"1 Plate: 42.18 x 28.92 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":327280,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1713/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":183721,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1713.JPG"}],"country":"United States","otherGeospatial":"New Madrid seismic zone","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a48e4b07f02db62387e","contributors":{"authors":[{"text":"Hopper, M. G.","contributorId":39389,"corporation":false,"usgs":true,"family":"Hopper","given":"M.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":262547,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Algermissen, S. T.","contributorId":39790,"corporation":false,"usgs":true,"family":"Algermissen","given":"S.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":262548,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":25126,"text":"cir930B - 1984 - International strategic minerals inventory summary report; chromium","interactions":[],"lastModifiedDate":"2018-11-05T10:20:12","indexId":"cir930B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"930","chapter":"B","title":"International strategic minerals inventory summary report; chromium","docAbstract":"Major world resources of chromium, a strategic mineral commodity, are described in this summary report of information in the International Strategic Minerals Inventory {ISMI}. ISMI is a cooperative data-collection effort of earth-science and mineral-resource agencies in Australia, Canada, the Federal Republic of Germany, the Republic of South Africa, and the United States of America. This report, designed to be of benefit to policy analysts, contains two parts. Part I presents an overview of the resources and potential supply of chromium on the basis of inventory information. Part II contains tables of some of the geologic information and mineral-resource and production data that were collected by ISMI participants.","language":"ENGLISH","publisher":"U.S. Dept. of the Interior, Geological Survey,","doi":"10.3133/cir930B","usgsCitation":"DeYoung, J., Lee, M.P., and Lipin, B., 1984, International strategic minerals inventory summary report; chromium: U.S. Geological Survey Circular 930, v. :ill. ;26 cm.; 41 p., https://doi.org/10.3133/cir930B.","productDescription":"v. :ill. ;26 cm.; 41 p.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":54106,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1984/0930b/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122560,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1984/0930b/report-thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49dbe4b07f02db5e0829","contributors":{"authors":[{"text":"DeYoung, J.H. Jr.","contributorId":86367,"corporation":false,"usgs":true,"family":"DeYoung","given":"J.H.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":193259,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lee, M. P.","contributorId":40198,"corporation":false,"usgs":true,"family":"Lee","given":"M.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":193257,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lipin, B. R.","contributorId":61031,"corporation":false,"usgs":true,"family":"Lipin","given":"B. R.","affiliations":[],"preferred":false,"id":193258,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":60254,"text":"mf1466C - 1984 - Mineral resource potential maps of the Jerry Peak, Jerry Peak West, and Boulder Creek Wilderness Study Areas, Custer County, Idaho","interactions":[],"lastModifiedDate":"2016-08-22T15:47:25","indexId":"mf1466C","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"1466","chapter":"C","title":"Mineral resource potential maps of the Jerry Peak, Jerry Peak West, and Boulder Creek Wilderness Study Areas, Custer County, Idaho","docAbstract":"<p>The U.S. Geological Survey and the U.S. Bureau of Mines made a geological and mineral survey of the Jerry Peak, Jerry Peak West, and Boulder Creek Wilderness Study Areas, Custer County, Idaho, from 1980 through 1983.</p>\n<p>The area is underlain chiefly by lavas and pyroclastic rocks of the Eocene Challis Volcanics. Paleozoic sedimentary rocks are exposed along the east border of the Jerry Peak Wilderness Study Area and in two small areas farther west in the Jerry Peak and Jerry Peak West Wilderness Study Areas. All the rocks locally are intricately faulted. No veins or pervasive hydrothermal alteration are associated with these faults.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/mf1466C","usgsCitation":"McIntyre, D.H., and Johnson, F.L., 1984, Mineral resource potential maps of the Jerry Peak, Jerry Peak West, and Boulder Creek Wilderness Study Areas, Custer County, Idaho: U.S. Geological Survey Miscellaneous Field Studies Map 1466, 35.36 x 52.45 inches, https://doi.org/10.3133/mf1466C.","productDescription":"35.36 x 52.45 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":182631,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1466C.PNG"},{"id":327353,"rank":1,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1466-C/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"50000","country":"United States","state":"Idaho","otherGeospatial":"Jerry Peak Wilderness 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H.","contributorId":45726,"corporation":false,"usgs":true,"family":"McIntyre","given":"D.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":263396,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, F. L.","contributorId":28236,"corporation":false,"usgs":true,"family":"Johnson","given":"F.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":263395,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":27083,"text":"wri844066 - 1984 - An assessment of nonpoint-source discharges, streamflow, and water quality in Onion River, Wisconsin","interactions":[],"lastModifiedDate":"2015-10-19T15:24:20","indexId":"wri844066","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"84-4066","title":"An assessment of nonpoint-source discharges, streamflow, and water quality in Onion River, Wisconsin","docAbstract":"<p>The Onion River in eastern Wisconsin was studied during the 1979 and 1980 water years to define the relationship between water quality and streamflow. Agricultural nonpoint-source discharges in the lower part of the Onion River are suspected of contributing significantly to degradation of water quality.</p>\n<p>Two streamflow water-quality monitoring stations were established on the Onion River, one at Hingham upstream of the affected area, and one near Sheboygan Falls downstream of the affected 272 pounds per square mile upstream of Hingham in the 1979 water year. Part of the high nutrient yields are due to point sources from Belgium Creek, which drains an area of 16.2 square miles. In the 1979 water year, point sources contributed an estimated 16,700 pounds of phosphorus or 45 percent of the total annual load downstream of Hingham, whereas, upstream of Hingham point sources contributed an estimated 2,200 pounds of phosphorus, or 18 percent of the total annual load. At Hingham during base flow, four of five phosphorus concentrations exceeded levels recommended by the U.S. Environmental Protection Agency; most concentrations during storm runoff exceeded these levels. At Sheboygan Falls, all phosphorus concentrations at base flow and most storm runoff concentrations also exceeded the Environmental Protection Agency criteria. All samples at both Hingham and Sheboygan Falls contained concentrations of un-ionized ammonia that were less than the U.S. Environmental Protection Agency's criteria (0.02 milligrams per liter), except the March 1980 samples. No samples exceeded the Wisconsin Department of Natural Resources criteria for un-ionized ammonia (0.04 milligrams per liter). area. Streamflow at Onion River at Hingham ranged from a minimum 7-day mean low flow (Q?) of 8.7 to a maximum discharge of 600 cubic feet per second; at Onion River near Sheboygan Falls streamflow ranged from a Q7 of 13 to a maximum discharge of 2,350 cubic feet per second. Based on discharges at the Sheboygan River at Sheboygan, these discharges ranged from about double the low flow that occurs on the average of once every 2 years, to discharges of between 5-and 10-year recurrence intervals. The average discharges at Hingham in the 1979 and 1980 water were 32.2 and 27.6 cubic feet per second, respectively. At Sheboygan Falls, the average discharges in the 1979 and 1980 water years were 94.2 and 55.2 cubic feet per second, respectively. Based on the average discharge at the Sheboygan River at Sheboygan, the 1979 discharge was 60 percent greater than average, and the 1980 discharge was about 5 percent less than average.</p>\n<p>Precipitation in the study area for the 1979 water year was 33.1 inches and for the 1980 water year it was 36.8 inches; these amounts are 3.3 inches and 7.0 inches, respectively, more than average.</p>\n<p>Suspended-sediment yields and, probably, phosphorus yields were slightly above average for both years because of greater than normal precipitation, and stream discharges that were greater than normal in 1979 and near normal in 1980. Suspended-sediment yields were 79.1 tons per square mile for the 1979 water year and 63.9 tons per square mile for the 1980 water year at Hingham, while downstream of Hingham the yields were 93.5 tons per square mile for the 1979 water year and 84.2 tons per square mile for the 1980 water year. Phosphorus yields were 331 pounds per square mile for the 1979 water year and 317 pounds per square mile for the 1980 water year at Hingham. Downstream of Hingham, the phosphorus yields were 656 pounds per square mile for the 1979 water year and 647 pounds per square mile for the 198Q water year.</p>\n<p>A population of bottom-dwelling carp resuspends the bottom sediments during its late spring and early summer active period, possibly causing high concentrations of suspended sediment and phosphorus.</p>\n<p>Nutrient yields and loading rates were highest downstream of Hingham. Nonpoint-source contribution of phosphorus amounted to 362 pounds per square mile downstream of Hingham compared to&nbsp;272 pounds per square mile upstream of Hingham in the 1979 water year.</p>\n<p>Part of the high nutrient yields are due to point sources from Belgium Creek, which drains an area of 16.2 square miles. In the 1979 water year, point sources contributed an estimated 16,700 pounds of phosphorus or 45 percent of the total annual load downstream of Hingham, whereas, upstream of Hingham point sources contributed an estimated 2,200 pounds of phosphorus, or 18 percent of the total annual load.</p>\n<p>At Hingham during base flow, four of five phosphorus concentrations exceeded levels recommended by the U.S. Environmental Protection Agency; most concentrations during storm runoff exceeded these levels. At Sheboygan Falls, all phosphorus concentrations at base flow and most storm runoff concentrations also exceeded the Environmental Protection Agency criteria.</p>\n<p>All samples at both Hingham and Sheboygan Falls contained concentrations of un-ionized ammonia that were less than the U.S. Environmental Protection Agency's criteria (0.02 milligrams per liter), except the March 1980 samples. No samples exceeded the Wisconsin Department of Natural Resources criteria for un-ionized ammonia (0.04 milligrams per liter).</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri844066","collaboration":"Prepared in cooperation with the Wisconsin Department of Natural Resources","usgsCitation":"Field, S.J., and Lidwin, R., 1984, An assessment of nonpoint-source discharges, streamflow, and water quality in Onion River, Wisconsin: U.S. Geological Survey Water-Resources Investigations Report 84-4066, vi, 78 p., https://doi.org/10.3133/wri844066.","productDescription":"vi, 78 p.","numberOfPages":"84","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":677,"text":"Wisconsin Water Science Center","active":true,"usgs":true}],"links":[{"id":55949,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1984/4066/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122885,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1984/4066/report-thumb.jpg"}],"country":"United States","state":"Wisconsin","county":"Ozaukee County, Sheboygan County","otherGeospatial":"Onion River","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -88.06503295898438,\n              43.7859669617277\n            ],\n            [\n              -88.15704345703124,\n              43.75125720420175\n            ],\n            [\n              -88.08563232421875,\n              43.62762639320158\n            ],\n            [\n              -87.88719177246094,\n              43.55352464927332\n            ],\n            [\n              -87.84393310546875,\n              43.555515149559746\n            ],\n            [\n              -87.8192138671875,\n              43.599289521300825\n            ],\n            [\n              -87.80548095703125,\n              43.65197548731187\n            ],\n            [\n              -87.77114868164062,\n              43.715534726205114\n            ],\n            [\n              -87.76016235351562,\n              43.76018449420188\n            ],\n            [\n              -87.81715393066406,\n              43.80083640601217\n            ],\n            [\n              -87.85903930664062,\n              43.777043519302175\n            ],\n            [\n              -87.98057556152344,\n              43.76365585841392\n            ],\n            [\n              -88.03688049316406,\n              43.77307711737606\n            ],\n            [\n              -88.06503295898438,\n              43.7859669617277\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db684dce","contributors":{"authors":[{"text":"Field, S. J.","contributorId":50540,"corporation":false,"usgs":true,"family":"Field","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":197527,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lidwin, R.A.","contributorId":33349,"corporation":false,"usgs":true,"family":"Lidwin","given":"R.A.","email":"","affiliations":[],"preferred":false,"id":197526,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":8214,"text":"ofr84147 - 1984 - Index of surface-water stations in Texas, January 1984","interactions":[],"lastModifiedDate":"2022-09-01T18:16:05.065422","indexId":"ofr84147","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-147","title":"Index of surface-water stations in Texas, January 1984","docAbstract":"<p>The U.S. Geological Survey's investigations of the water resources of Texas are conducted in cooperation with the Texas Department of Water Resources, river authorities, cities, counties, U.S. Army Corps of Engineers, U.S. Bureau of Reclamation, International Boundary and Water Commission, and others.</p>\n<p>Investigations are under the general direction of C. W. Boning, District Chief, Texas District. The Texas District office is located in the Federal Building, 300 East 8th Street, Austin, Texas 78701.</p>\n<p>As of January 1, 1984, 399 stream-gaging, 86 reservoir-contents, 19 stage, 2 periodic discharge through range, 42 flood-hydrograph partial-record, 15 floodprofile partial-record, 34 low-flow partial-record, 11 crest-stage partial-record, 11 tide-level , 60 daily chemical-qual ity, 27 continuous-recording water-quality, 187 periodic chemical-qual ity, 175 periodic organic-quality, 60 pesticides, 1 sediment, 43 periodic sediment, 109 periodic biological, 28 continuous-recording water temperature, and 37 national stream-quality accounting network stations were in operation. Plate 1 shows the location of surface-water streamflow or reservoircontent and chemical-qual ity or sediment stations in Texas. Plate 2 shows the location of partial-record surface-water stations.</p>\n<p>This index shows the station number and name, latitude and longitude, type of data collected, and the office principally responsible for the data collection (table 1). An 8-digit permanent numerical designation for gaging stations has been adopted on a nationwide basis; stations are numbered and listed in downstream order. In the downstream direction along the main stem, all stations on a tributary entering above a main-stem station are listed before that station. A tributary entering between two main-stem stations is listed between them. A similar order is followed in listing stations on first rank, second rank, and other ranks of tributaries. To indicate the rank of any tributary on which a gaging station is situated and the stream to which it is an immediate tributary, each indention in the listing of gaging stations represent one rank. This downstream order and system of indention show which gaging stations are on tributaries between any two stations on a main stem and the rank of the tributary on which each gaging station is situated. On plates 1 and 2 the 8-digit station number is abbreviated because of space limitation.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Austin, TX","doi":"10.3133/ofr84147","usgsCitation":"Carrillo, E., and Buckner, H., 1984, Index of surface-water stations in Texas, January 1984: U.S. Geological Survey Open-File Report 84-147, Report: ii, 16 p.; 2 Plates: 18.51 x 17.15 inches and 18.39 x 17.55 inches, https://doi.org/10.3133/ofr84147.","productDescription":"Report: ii, 16 p.; 2 Plates: 18.51 x 17.15 inches and 18.39 x 17.55 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":406082,"rank":5,"type":{"id":36,"text":"NGMDB Index 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,{"id":40338,"text":"ofr84587 - 1984 - Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon","interactions":[{"subject":{"id":40338,"text":"ofr84587 - 1984 - Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon","indexId":"ofr84587","publicationYear":"1984","noYear":false,"title":"Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon"},"predicate":"SUPERSEDED_BY","object":{"id":63495,"text":"gp969 - 1986 - Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon","indexId":"gp969","publicationYear":"1986","noYear":false,"title":"Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon"},"id":1}],"supersededBy":{"id":63495,"text":"gp969 - 1986 - Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon","indexId":"gp969","publicationYear":"1986","noYear":false,"title":"Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon"},"lastModifiedDate":"2024-01-22T21:06:48.839996","indexId":"ofr84587","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-587","title":"Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon","docAbstract":"<p>This report is one in a series resulting from the U.S. Geological Survey's Snake River Plain RASA (Regional Aquifer System Analysis) study that began in October 1979.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr84587","usgsCitation":"Whitehead, R., 1984, Compilation of selected geophysical references for the Snake River plain, Idaho and eastern Oregon: U.S. Geological Survey Open-File Report 84-587, Report: 1 p.; 1 Plate: 54.96 x 35.97 inches, https://doi.org/10.3133/ofr84587.","productDescription":"Report: 1 p.; 1 Plate: 54.96 x 35.97 inches","costCenters":[],"links":[{"id":424703,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1984/0587/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":424702,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0587/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":135467,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0587/report-thumb.jpg"}],"scale":"500000","country":"United States","state":"Idaho, Oregon","otherGeospatial":"Snake River plain","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"coordinates\": [\n          [\n            [\n              -119.79353516529073,\n              44.75814253835162\n            ],\n            [\n              -119.79353516529073,\n              42.00600446943071\n            ],\n            [\n              -111.1325958997702,\n              42.00600446943071\n            ],\n            [\n              -111.1325958997702,\n              44.75814253835162\n            ],\n            [\n              -119.79353516529073,\n              44.75814253835162\n            ]\n          ]\n        ],\n        \"type\": \"Polygon\"\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1de4b07f02db6a9722","contributors":{"authors":[{"text":"Whitehead, R.L.","contributorId":34891,"corporation":false,"usgs":true,"family":"Whitehead","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":223291,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":11641,"text":"ofr83948 - 1984 - Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States","interactions":[{"subject":{"id":11641,"text":"ofr83948 - 1984 - Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States","indexId":"ofr83948","publicationYear":"1984","noYear":false,"title":"Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States"},"predicate":"SUPERSEDED_BY","object":{"id":2967,"text":"wsp2276 - 1986 - Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States","indexId":"wsp2276","publicationYear":"1986","noYear":false,"title":"Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States"},"id":1}],"supersededBy":{"id":2967,"text":"wsp2276 - 1986 - Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States","indexId":"wsp2276","publicationYear":"1986","noYear":false,"title":"Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States"},"lastModifiedDate":"2021-01-26T20:35:22.176536","indexId":"ofr83948","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"83-948","title":"Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States","docAbstract":"<p>No abstract available.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr83948","usgsCitation":"Wetzel, K.L., and Bettandorff, J., 1984, Techniques for estimating streamflow characteristics in the Eastern and Interior coal provinces of the United States: U.S. Geological Survey Open-File Report 83-948, Report: v, 95 p.; 2 Plates: 28.99 x 28.04 inches and 27.71 x 28.21 inches, https://doi.org/10.3133/ofr83948.","productDescription":"Report: v, 95 p.; 2 Plates: 28.99 x 28.04 inches and 27.71 x 28.21 inches","costCenters":[],"links":[{"id":145105,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0948/report-thumb.jpg"},{"id":382613,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0948/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":382615,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1983/0948/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":382614,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1983/0948/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685a4a","contributors":{"authors":[{"text":"Wetzel, K. L.","contributorId":14418,"corporation":false,"usgs":true,"family":"Wetzel","given":"K.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":163490,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bettandorff, J.M.","contributorId":67499,"corporation":false,"usgs":true,"family":"Bettandorff","given":"J.M.","email":"","affiliations":[],"preferred":false,"id":163491,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":38647,"text":"pp1151D - 1984 - Stratigraphy and structure of the western Kentucky fluorspar district","interactions":[],"lastModifiedDate":"2012-02-02T00:09:58","indexId":"pp1151D","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1151","chapter":"D","title":"Stratigraphy and structure of the western Kentucky fluorspar district","docAbstract":"The western Kentucky fluorspar district is part of the larger Illinois-Kentucky fluorspar district, the largest producer of fluorspar in the United States. This report is based largely on data gathered from 1960 to 1974 during the U.S. Geological Survey-Kentucky Geological Survey cooperative geologic mapping program of Kentucky. It deals chiefly with the stratigraphy and structure of the district and, to a lesser extent, with the fluorspar-zinc-lead-barite deposits. \r\n\r\nSedimentary rocks exposed in the district range in age from Early Mississippian (Osagean) to Quaternary. Most rocks exposed at the surface are Mississippian in age; two-thirds are marine fossiliferous limestones, and the remainder are shales, siltstones, and sandstones. Osagean deep-water marine silty limestone and chert are present at the surface in the southwestern corner of the district. Meramecian marine limestone is exposed at the surface in about half the area. Chesterian marine and fluvial to fluviodeltaic clastic sedimentary rocks and marine limestone underlie about one-third of the area. The total sequence of Mississippian rocks is about 3,000 ft thick. \r\n\r\nPennsylvanian rocks are dominantly fluvial clastic sedimentary rocks that change upward into younger fluviodeltaic strata. Pennsylvanian strata of Morrowan and Atokan age are locally thicker than 600 ft along the eastern and southeastern margin and in the major grabens of the district where they have been preserved from erosion. \r\n\r\nCretaceous and Tertiary sediments of the Mississippi embayment truncate Paleozoic formations in and near the southwestern corner of the district and are preserved mostly as erosional outliers. The deposits are Gulfian nonmarine gravels, sands, and clays as much as 170 ft thick and upper Pliocene fluvial continental deposits as thick as 45 ft. Pleistocene loess deposits mantle the upland surface of the district, and Quaternary fluvial and fluviolacustrine deposits are common and widespread along the Ohio and Cumberland Rivers and their major tributaries. \r\n\r\nMany mafic dikes and a few mafic sills are present. The mafic rocks are mostly altered mica peridotites or lamprophyres that are composed of carbonate minerals, serpentine, chlorite, and biotite and contain some hornblende, pyroxene, and olivine. Most of the dikes are in a north-north west-trending belt 6 to 8 mi wide and strike N. 20 0 -30 0 W. The dikes dip from 80 0 to 90 0 and are commonly 5 to 10 ft wide. Radioisotopic study indicates that the dikes are Early Permian in age. \r\n\r\nThe district is just southeast of the intersection of the east-trending Rough Creek-Shawneetown and northeast-trending New Madrid fault systems. The district's principal structural features are a northwest-trending domal anticline, the Tolu Arch, and a series of steeply dipping to nearly vertical normal faults and fault zones that trend dominantly northeastward and divide the area into elongated northeast-trending grabens and horsts. Formation of these grabens and horsts was one of the major tectonic events in the district. Vertical displacement may be as much as 3,000 ft but commonly ranges from a few feet to a few hundred feet; no substantial horizontal movement is believed to have taken place. Many cross faults having only a few feet of displacement trend northwestward and are occupied at places by mafic dikes. Faulting was mostly post-Early Permian to pre-middle Cretaceous in age. \r\n\r\nMany theories have been advanced to explain the structural history of the district. A generally acceptable overall hypothesis that would account for all the structural complexities, however, is still lacking. Useful structural data, such as the structural differences between the grabens and the horsts, have been obtained, however, from the recently completed geologic mapping. Mapping also has more clearly shown the alinement of the Tolu Arch, the belt of dikes, and an unusually deep graben (the Griffith Bluff graben); this alinement suggests that possibl","language":"ENGLISH","doi":"10.3133/pp1151D","usgsCitation":"Trace, R.D., and Amos, D., 1984, Stratigraphy and structure of the western Kentucky fluorspar district: U.S. Geological Survey Professional Paper 1151, p. D1-D41; 1 plate in pocket, https://doi.org/10.3133/pp1151D.","productDescription":"p. D1-D41; 1 plate in pocket","costCenters":[],"links":[{"id":119900,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1151d/report-thumb.jpg"},{"id":65478,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1151d/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65479,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1151d/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a7fee","contributors":{"authors":[{"text":"Trace, R. D.","contributorId":47004,"corporation":false,"usgs":true,"family":"Trace","given":"R.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":220215,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Amos, D.H.","contributorId":75600,"corporation":false,"usgs":true,"family":"Amos","given":"D.H.","email":"","affiliations":[],"preferred":false,"id":220216,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":27841,"text":"wri834207 - 1984 - Evaluation of the potential for artificial ground-water recharge in eastern San Joaquin County, California — Phase 2","interactions":[],"lastModifiedDate":"2022-01-18T22:40:21.549985","indexId":"wri834207","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"83-4207","title":"Evaluation of the potential for artificial ground-water recharge in eastern San Joaquin County, California — Phase 2","docAbstract":"In response to the increasing demand on water supplies and declining water levels in eastern San Joaquin County, the U.S. Geological Survey, in cooperation with the San Joaquin County Flood Control and Water Conservation District, is evaluating the potential for artificially recharging the aquifer system in eastern San Joaquin County, Calif. Phase 1 of this study evaluated the geologic and hydrological conditions in the area and selected 20 drill sites in three areas of high potential for artificial recharge of the aquifer system. In phase 2, test holes were drilled. This report is on phase 2, and summarizes the data collected during the drilling and evaluates the suitability of the drilled areas for their potential for artificial recharge. Two areas seem to have a fair potential for artificial recharge of the aquifer system using the basin-spreading method: (1) The flood plain area along the Mokelumne River north of Lockeford, and (2) an area northeast of Linden along the Calaveras River. (USGS)","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri834207","usgsCitation":"Ireland, R.L., 1984, Evaluation of the potential for artificial ground-water recharge in eastern San Joaquin County, California — Phase 2: U.S. Geological Survey Water-Resources Investigations Report 83-4207, Report: iv, 28 p.; 2 Plates: 29.24 × 35.17 inches and 34.60 × 27.49 inches, https://doi.org/10.3133/wri834207.","productDescription":"Report: iv, 28 p.; 2 Plates: 29.24 × 35.17 inches and 34.60 × 27.49 inches","costCenters":[],"links":[{"id":56669,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1983/4207/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":56668,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1983/4207/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":394484,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_35850.htm"},{"id":56667,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1983/4207/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123318,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1983/4207/report-thumb.jpg"}],"country":"United States","state":"California","county":"San Joaquin County","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -121.25,\n              37.8740\n            ],\n            [\n              -120.917,\n              37.8740\n            ],\n            [\n              -120.917,\n              38.25\n            ],\n            [\n              -121.25,\n              38.25\n            ],\n            [\n              -121.25,\n              37.8740\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa1fc","contributors":{"authors":[{"text":"Ireland, R. L.","contributorId":89893,"corporation":false,"usgs":true,"family":"Ireland","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":198763,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":25971,"text":"wri844194 - 1984 - Evaluation of the hydrologic system and potential effects of mining in the Dickinson lignite area, eastern slope and western Stark and Hettinger counties, North Dakota","interactions":[],"lastModifiedDate":"2018-02-14T15:41:55","indexId":"wri844194","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"84-4194","title":"Evaluation of the hydrologic system and potential effects of mining in the Dickinson lignite area, eastern slope and western Stark and Hettinger counties, North Dakota","docAbstract":"<p>The investigation of the water resources of the Dickinson lignite area, an area of about 500 square miles, was undertaken to define the hydrologic system of the area and to project probable effects of coal mining on the system.</p><p>Aquifers occur in sandstone beds in: the Fox Hills Sandstone and the lower Hell Creek Formation of Cretaceous age, the upper Hell Creek Formation of Cretaceous age and the lower Ludlow Member of the Fort Union Formation of Tertiary age, and the upper Ludlow and lower Tongue River Members of the Fort Union Formation of Tertiary age. Aquifers also occur in the sandstone and lignite lenses in the upper Tongue River Member and the Sentinel Butte Member of the Fort Union Formation. </p><p>Depths to the Fox Hills-lower Hell Creek aquifer system range from about 1,300 to 1,710 feet. Well yields range from 18 to 100 gallons per minute. The water is soft and is a sodium bicarbonate type. Dissolvedsolids concentrations in samples collected from the aquifer system ranged from 1,230 to 1,690 milligrams per liter.</p><p>Depths to the upper Hell Creek-lower Ludlow aquifer system range from about 720 to 1,040 feet. Well yields generally are less than 30 gallons per minute but may be as much as 150 gallons per minute. The water is soft and a sodium bicarbonate type. Dissolved-solids concentrations in samples collected from the aquifer system ranged from 1,010 to 1,450 milligrams per liter.</p><p>Depths to the upper Ludlow-lower Tongue River aquifer system range from about 440 to 713 feet. Well yields may range from about 1 to 100 gallons per minute. The water generally is soft and a sodium bicarbonate type but may be moderately hard and a sulfate type in the southwestern part of the area. Dissolved-solids concentrations in samples collected from the aquifer system ranged from 995 to 1,990 milligrams per liter. </p><p>Depths to the upper Tongue River-Sentinel Butte aquifer system range from near land surface to about 530 feet below land surface. Well yields generally range from about 1 to 185 gallons per minute. Yields from the lignite parts of the system range from about 2 to 60 gallons per minute. The water generally is a sodium bicarbonate type, but locally sulfate is the dominant anion. Dissolved-solids concentrations in samples collected from the aquifer system generally ranged from 574 to 2,720 milligrams per liter.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri844194","usgsCitation":"Armstrong, C.A., 1984, Evaluation of the hydrologic system and potential effects of mining in the Dickinson lignite area, eastern slope and western Stark and Hettinger counties, North Dakota: U.S. Geological Survey Water-Resources Investigations Report 84-4194, Report: v, 35 p.; Plate: 22.55 x 19.31 inches, https://doi.org/10.3133/wri844194.","productDescription":"Report: v, 35 p.; Plate: 22.55 x 19.31 inches","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":123870,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1984/4194/report-thumb.jpg"},{"id":54717,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1984/4194/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":54718,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1984/4194/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"North Dakota","county":"Hettinger County, Stark County","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a08e4b07f02db5fa3b1","contributors":{"authors":[{"text":"Armstrong, C. A.","contributorId":66231,"corporation":false,"usgs":true,"family":"Armstrong","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":195565,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":38513,"text":"pp1342 - 1984 - The evolution of the southern California uplift, 1955 through 1976","interactions":[],"lastModifiedDate":"2017-04-25T15:11:50","indexId":"pp1342","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1342","title":"The evolution of the southern California uplift, 1955 through 1976","docAbstract":"<p>The southern California uplift culminated in 1974 as a 150- km-wide crustal swell that extended about 600 km eastward and east-southeastward from Point Arguello to the Colorado River and Salton Sea, respectively; it was characterized by remarkably uniform height changes between 1959 and 1974 of 0.30-0.35 m over at least half of its 60,000-70,000 km<sup>2</sup> area. At its zenith, the uplift included virtually the entire Transverse Ranges geologic province and parts of the Coast Ranges, San Joaquin Valley, Sierra Nevada, Basin and Range, Mojave Desert, Peninsular Ranges, and Salton Trough provinces. The alinement of the western part of the uplift closely paralleled the east-trending Transverse Ranges, whereas the southern flank of the eastern lobe roughly coincided with the west-northwest-trending San Andreas fault. The position and configuration of the uplift associate it with a singularly complex section of the boundary between the North American and Pacific plates that has certainly sustained major modification during the past 5 million years and probably during the past 1 million years. </p><p>Surface deformation can be categorized as tectonic or nontectonic. Nontectonic vertical displacements associated with the activities of man have overwhelmed natural compaction and areally significant soil expansion in the southern California area. Because tectonic displacements are implicitly defined as those that cannot be otherwise explained, those vertical movements that can be reasonably attributed to artificial processes have been subtracted from our reconstructed configurations of the uplift. Hence this reconstruction has necessarily included the assembly and evaluation of an enormous volume of data on oil-field operations, changes in ground-water levels, and measured subsidence (or rebound) associated with changes in the underground fluid regimen. </p><p>Measured changes in height at various stages in the evolution of the uplift have been based chiefly on first-order levelings carried out between 1953 and 1976. Exceptions to this generalization consist largely of the results of pre-1953 surveys through the western Transverse Ranges and the eastern Mojave Desert. Errors in measured height differences derive from blunders, systematic survey errors, random survey errors, improperly formulated orthometric corrections, and intrasurvey movement; the last of these has created the most serious problems encountered in our reconstruction of the basic data. A variety of independent tests indicate that survey error associated with the utilized levelings was generally small and fell largely within the predicted random-error range. Moreover, the redundancy and coherence displayed by the entire data set provide convincing evidence of survey accuracy and the virtual absence of height- and slope-dependent error in particular. </p><p>Our reconstructions of the changing configuration of the uplift derive chiefly from comparisons among sequentially developed observed elevations along the same route. Most of the observed elevations from which the vertical displacements were computed have been reconstructed with respect to bench mark Tidal 8, San Pedro, as invariant in height. Because the San Pedro tide station has been characterized by a history of modest relative uplift, vertical displacements referred to this station are biased slightly toward the appearance of subsidence. Where the observed elevations cannot be conveniently tied to Tidal 8, they have been referred to secondary control points whose history with respect to Tidal 8 can be independently established. Each of the lines of observed elevation changes provides, accordingly, a section athwart or along the axis of the uplift from which the changes in the configuration of the uplift can be roughly generalized. Because relatively few surveys were run in 1955, which we choose as a representative temporal datum, we have commonly incorporated the results of earlier or of somewhat later levelings as the equivalents of 1955 surveys. Although this procedure introduces a certain subjectivity, the probable equivalence between the results of these earlier or later surveys with those that would have been obtained had this leveling been carried out in 1955, usually can be independently tested. Wherever the calculated vertical displacements are based on comparisons between the results of levelings over different routes, the observed elevations have been orthometrically corrected to agree with those that would have been produced had each of these surveys been along the same route. </p><p>The growth of the southern California uplift consisted of two well-defined spasms of positive movement, the second of which was closely followed by partial collapse. Our reconstruction, although it clearly errs in detail, indicates that the uplift, together with marginal and apparently ephemeral tectonic subsidence, nucleated in the west-central Transverse Ranges near Ozena, sometime between the spring of 1959 and the spring of 1960. The uplift expanded rapidly eastward (and probably westward as well), and by the fall of 1961 much of the Transverse Ranges and the Mojave Desert at least as far east as Twentynine Palms had risen by as much as 0.25 m. Between 1962 and 1972 the area included by the initially developed (1959-61) uplift sustained additional but clearly decelerating uplift accompanied locally by oscillatory displacements. Between 1972/ 73 and 1974 a second crustal spasm extended the uplift eastward to the Colorado River and elevated much of the eastern Mojave Desert by values that equaled or exceeded those developed within the western lobe. Between 1974 and 1976, at least the central part of the uplift sustained partial collapse that nowhere amounted to less than 50 percent of the cumulative uplift since 1959. Whether this collapse affected the entire uplift is conjectural, but we now recognize well-defined evidence of major down-to-the-north tilting that must have occurred within the eastern part of the uplift at some time between 1974 and 1976. </p><p>Accumulating evidence indicates that nearly all the area included with the southern California uplift underwent similar uplift and partial collapse during the early part of the 20th century. Thus we infer that the recent uplift represents but a single event in an ongoing, more or less cyclic deformational process characterized by a period of about 50 years. Even though less than two full cycles are expressed in the geodetic&nbsp;record, the cumulative rate of uplift near the center of the recent uplift probably has averaged about 5 mm/yr, a value that is roughly consistent with the uplift rates that have been deduced for the late Quaternary emergent marine terraces along the south flank of the Transverse Ranges. </p><p>Although the evolution of the recent uplift is relatively well defined, its correlation with the regional seismicity is poorly defined. A comparison between the occurrence of southern California earthquakes of magnitude ≥4 during the period 1932 to 1976 with the 1974 configuration of the uplift demonstrates the existence of (1) relatively aseismic areas within the western lobe of the uplift (in the western Transverse Ranges), in the central part of the uplift (in the western Mojave Desert), and along an east-trending zone that extends into the eastern Mojave athwart the south flank of the uplift (north of the Salton Sea) and (2) localized concentrations of seismic activity along the flanks of the uplift. Moreover, 9 of the 10 largest earthquakes recorded within or around the area of the southern California uplift during the period 1932 to 1976 (the 1933 Long Beach, the 1941 Santa Barbara, the 1946 Walker Pass, the 1947 Manix, the 1948 Desert Hot Springs, and the four major 1952 Kern County shocks) occurred before the inception of the uplift in 1959 or 1960. </p><p>The area embraced by the southern California uplift has been identified with geodetically defined horizontal strain, part of which may have accumulated as a major north-south contractional event that roughly coincided with the first spasm of uplift. Nonetheless, continuing contractional strain associated with regionally developed partial collapse argues that the uplift cannot be fully explained simply as the vertical expression of continuing north-south compression. Consideration of the two well-defined historical episodes of uplift and partial collapse indicate that the southern California uplift may be the product of decoupling and viscous flow beneath the seismogenic zone, presumably driven by continuing motion between the irregularly margined plates south of the great bend of the San Andreas fault. Because the magnitude of the maximum uplift associated with each episode was approximately the same, there may be some threshold value above which collapse (viscous flow) may ensue; the absence of total collapse may be a function of precollapse strain hardening within the postulated subseismogenic viscoelastic layer.</p>","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/pp1342","usgsCitation":"Castle, R.O., Elliot, M.R., Church, J.P., and Wood, S.H., 1984, The evolution of the southern California uplift, 1955 through 1976: U.S. Geological Survey Professional Paper 1342, Report: vii, 136 p.; 16 Plates: 48 x 50.5 inches or less, https://doi.org/10.3133/pp1342.","productDescription":"Report: vii, 136 p.; 16 Plates: 48 x 50.5 inches or less","costCenters":[],"links":[{"id":65240,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1342/plate-07.pdf","text":"Plate 7","size":"973.46 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,{"id":60900,"text":"mf1615B - 1984 - Aeromagnetic, Bouguer gravity, and interpretation maps of the Sheep Hole-Cadiz Wilderness Study Area (CDCA-305), San Bernardino County, California","interactions":[],"lastModifiedDate":"2016-08-23T09:28:49","indexId":"mf1615B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"1615","chapter":"B","title":"Aeromagnetic, Bouguer gravity, and interpretation maps of the Sheep Hole-Cadiz Wilderness Study Area (CDCA-305), San Bernardino County, California","docAbstract":"<p><span>The Federal Land Policy and Management&nbsp;Act (Public Law 94-579, October 21, 1976) requires the U.S. Geological Survey and the U.S. Bureau of Mines to conduct mineral surveys on certain areas to determine their mineral resource potential. Results must be made available to the public and be submitted to the President and the Congress. These maps presents the results of a mineral survey of the&nbsp;Sheep Hole-Cadiz Wilderness Study Area (CDCA-305), California Desert Conservation Area, San Bernardino County, California.</span></p>\n<p><span>The&nbsp;U.S. Bureau of Mines conducted a mineral survey of the&nbsp;Sheep Hole-Cadiz Wilderness Study Area, which encompasses approximately 200,000 acres including enclosed private lands, in south-central San Bernardino County, California.&nbsp;The&nbsp;U.S. Bureau of Mines studied the mineral resources of mines, prospects, and mineralized areas; geologic, geochemical, and geophysical investigations were conducted by the&nbsp;U.S. Geological Survey.</span></p>\n<p><span>The study area is located in the Mojave Desert 13 miles east of Amboy, California, 20 miles east of Twentynine Palms, California, and 90 miles east of San Bernardino, and encompasses parts of the Dale Lake, Bristol Lake, Cadiz Valley and Cadiz Lake 15-minute quadrangles. Its borders are defined by the Amboy Road and a gas pipeline service road on the northwest, the unimproved Cadiz Valley access road on the east, State Route 62 along the south, and the Iron Age mine road and an unimproved powerline service road on the west. Major access from the east and west is provided by State Route 62 and access from the north is provided by the Amboy Road.</span></p>\n<p><span>Companion reports to this one describe the mineral resource potential (March and others, 1982), the geology (Howard and John, 1984), and hydrothermal alteration&nbsp;studies (Raines, 1983).</span></p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf1615B","collaboration":"Prepared in cooperation with the U.S. Bureau of Land Management","usgsCitation":"Simpson, R., Bracken, R.E., and Stierman, D., 1984, Aeromagnetic, Bouguer gravity, and interpretation maps of the Sheep Hole-Cadiz Wilderness Study Area (CDCA-305), San Bernardino County, California: U.S. Geological Survey Miscellaneous Field Studies Map 1615, 4 plates: 47.80 x 42.15 inches or smaller, https://doi.org/10.3133/mf1615B.","productDescription":"4 plates: 47.80 x 42.15 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":327494,"rank":1,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1615-B/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":327495,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1615-B/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":327496,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1615-B/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":327497,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1615-B/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":180166,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1615B.PNG"}],"country":"United States","state":"California","county":"San Bernardino County","otherGeospatial":"California Desert Conservation Area, Mojave Desert, Sheep Hole-Cadiz Wilderness Study Area","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -115.75,34 ], [ -115.75,34.5 ], [ -115.25,34.5 ], [ -115.25,34 ], [ -115.75,34 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae4e4b07f02db689bdc","contributors":{"authors":[{"text":"Simpson, R.W.","contributorId":76738,"corporation":false,"usgs":true,"family":"Simpson","given":"R.W.","email":"","affiliations":[],"preferred":false,"id":264581,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bracken, R. E.","contributorId":98316,"corporation":false,"usgs":true,"family":"Bracken","given":"R.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":264582,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stierman, D.J.","contributorId":54621,"corporation":false,"usgs":true,"family":"Stierman","given":"D.J.","email":"","affiliations":[],"preferred":false,"id":264580,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":13537,"text":"ofr85512 - 1984 - Analytical results, geology, and sample locality map of mercury-sulfur-gypsum mineralization at Crater, Inyo County, California","interactions":[],"lastModifiedDate":"2016-02-01T13:54:45","indexId":"ofr85512","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"85-512","title":"Analytical results, geology, and sample locality map of mercury-sulfur-gypsum mineralization at Crater, Inyo County, California","docAbstract":"<p>The Crater mercury-su l fur-gypsum ~ineral ized area is located in east-central California along the crest of the Last Chance Range, west of the north end of Death Valley (fig. 1). The area is in the northwest quarter of the Last Chance Range 15-minute quadrangle and occupies the area between 117 39 and 117 45 longitude and 37 10 and 37 15 latitudP.. The area studied lies between 5000 ( 1525 m) and 6000 ( 1830 m) feet above sea level. Relief isgenerally moderate but can be extreme in some places, as at Hanging Rock Canyon (plate 1). The climate is arid, and there are no active streams in the area. The range fronts east and west of the area are precipitous and incised by many steep canyons, whereas the range crest has relatively low relief. The old abandoned town and mine site of Crater 1 ie in this area of low relief. Access to the Crater area is by paved and dirt roads from Big Pine to the west or from the north end of the Death Valley National Monument to the southeast.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr85512","usgsCitation":"Erickson, M.S., Marsh, S., and Roemer, T.A., 1984, Analytical results, geology, and sample locality map of mercury-sulfur-gypsum mineralization at Crater, Inyo County, California: U.S. Geological Survey Open-File Report 85-512, 25 p., https://doi.org/10.3133/ofr85512.","productDescription":"25 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,{"id":29589,"text":"wri834237 - 1984 - Water levels and water-level changes in the Prairie du Chien-Jordan and Mount Simon-Hinckley aquifers, Twin Cities metropolitan area, Minnesota, 1971-80","interactions":[],"lastModifiedDate":"2018-04-02T10:23:19","indexId":"wri834237","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"83-4237","title":"Water levels and water-level changes in the Prairie du Chien-Jordan and Mount Simon-Hinckley aquifers, Twin Cities metropolitan area, Minnesota, 1971-80","docAbstract":"<p>The ground-water system in the Twin Cities Metropolitan Area includes five aquifers; two of these aquifers the Prairie du Chien-Jordan and the Mount Simon-Hinckley supply about 80 percent and 10 percent, respectively, of the ground water pumped for public supply. Water levels and changes in water levels in these two aquifers differ greatly in the Twin Cities Metropolitan Area. The Mississippi, Minnesota, and St. Croix Rivers are in hydraulic connection with and influence the pattern of flow in the upper aquifer, the Prairie du Chien-Jordan. Water generally flows toward these streams from water-level highs northeast, northwest, and south of Minneapolis and St. Paul. Consequently, heavy pumping has caused only localized cones of depression in the potentiometric surface of this aquifer. In contrast, the Mount Simon-Hinckley, which has only a slight hydraulic connection to the streams, is greatly influenced by pumping. Pumping in the urban centers of Minneapolis and St. Paul has caused a large cone of depression in the Mount Simon-Hinckley potentiometric surface. During 1971, the measurable cone was centered in eastcentral Hennepin County, was about 25 miles in diameter, and was as much as 150 feet deep at its center.</p>\n<p>Between 1971 and 1980, average water levels in the Prairie du Chien-Jordan aquifer changed less than 5 feet in most of the study area, but rose or declined as much as 25 feet locally in response to pumpage and recharge. During this period, seasonal declines of water levels from winter to summer lessened, and the area where these declines exceeded 10 feet decreased.</p>\n<p>In contrast, between 1971 and 1980, average water levels in the Mount Simon-Hinckley aquifer rose as much as 60 feet in the center of the cone of depression in response to decreased pumping. Also, the measurable cone of depression contracted from about 25 miles to about 15 miles in diameter. However, because of increased summer pumping due to below-average precipitation during 1980, seasonal water levels declined much more and over a wider area during 1980 than in 1971.</p>\n<p>Water-level data suggest that (1) little variation in annual pumpage between 1971 and 1980 from the Prairie du Chien-Jordan aquifer produced generally stable water levels in that aquifer, (2) decreased annual pumpage from the Mount Simon-Hinckley aquifer from 1971 to 1980 caused water levels in that aquifer to rise, and (3) a greater seasonal component of pumpage from the Mount Simon-Hinckley aquifer than from the Prairie du Chien-Jordan produced larger and more widespread seasonal water-level declines in the Mount Simon-Hinckley than in the Prairie du Chien-Jordan, particularly during dry years.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"St. Paul, MN","doi":"10.3133/wri834237","collaboration":"Prepared in cooperation with the Metropolitan Council of the Twin 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,{"id":59138,"text":"mf1101B - 1984 - Summary geochemical maps, Hoover Wilderness and adjacent study area, Mono and Tuolumne counties, California","interactions":[],"lastModifiedDate":"2013-12-04T14:04:30","indexId":"mf1101B","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"1101","chapter":"B","title":"Summary geochemical maps, Hoover Wilderness and adjacent study area, Mono and Tuolumne counties, California","docAbstract":"The Hoover Wilderness and the adjacent Hoover Extension (East), Hoover Extension (West), and Cherry Creek A Roadless Areas (the adjacent study area) encompass approximately 153,900 acres (241 mi<sup>2</sup>; 623 km<sup>2</sup>) in the Inyo, Stanislaus, and Toiyabe Naitonal Forests, Mono and Tuolumne Counties, Calif. These two areas lie along and mostly east of the crest of the Sierra Nevada, along the north and east sides of Yosemite National Park. Elevations vary from a high of 12,446 ft (3,793 m) on the crest of the Sierra Nevada to a low of about 6,500 ft (1,981 m) near the Bridgeport Ranger Station. Access to the Hoover Wilderness and adjacent study area is by U.S. Highway 395, California State Highways 108 (Sonora Pass) and 120 (Tioga Pass), and by other paved and graded roads that lead off of these U.S. and State highways.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/mf1101B","usgsCitation":"Chaffee, M., Hill, R.H., and Sutley, S.J., 1984, Summary geochemical maps, Hoover Wilderness and adjacent study area, Mono and Tuolumne counties, California: U.S. Geological Survey Miscellaneous Field Studies Map 1101, 3 Plates: 38.32 x 43.82 or smaller, https://doi.org/10.3133/mf1101B.","productDescription":"3 Plates: 38.32 x 43.82 or smaller","costCenters":[],"links":[{"id":182994,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/1101b/report-thumb.jpg"},{"id":278816,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1101b/plate-2.pdf"},{"id":278817,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1101b/plate-3.pdf"},{"id":278815,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1101b/plate-1.pdf"}],"scale":"62500","country":"United States","state":"California","county":"Mono County;Tuolumne County","otherGeospatial":"Hoover Wilderness;Inyo National Forest;Stanislaus National Forest;Toiyabe National Forest;Yosemite National Park","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -119.75,37.916667 ], [ -119.75,38.383333 ], [ -119.166667,38.383333 ], [ -119.166667,37.916667 ], [ -119.75,37.916667 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b04e4b07f02db699583","contributors":{"authors":[{"text":"Chaffee, M.A.","contributorId":108049,"corporation":false,"usgs":true,"family":"Chaffee","given":"M.A.","affiliations":[],"preferred":false,"id":261495,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hill, R. H.","contributorId":57059,"corporation":false,"usgs":true,"family":"Hill","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":261493,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sutley, S. J.","contributorId":91484,"corporation":false,"usgs":true,"family":"Sutley","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":261494,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":56652,"text":"fwsobs82_10_64 - 1984 - Habitat Suitability Index Models and Instream Flow Suitability Curves: White sucker","interactions":[],"lastModifiedDate":"2022-02-09T15:14:30.028474","indexId":"fwsobs82_10_64","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":20,"text":"FWS/OBS","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"82/10.64","subseriesTitle":"Habitat Suitability Index","title":"Habitat Suitability Index Models and Instream Flow Suitability Curves: White sucker","docAbstract":"<p>The white sucker (Catostomus commersoni) is a highly adaptable, freshwater fish species found in lacustrine and riverine environments from the Mackenzie River, Hudson Bay drainage, and the Labrador Peninsula; south along the Atlantic Coast to western Georgia; along the northern extremes of the Gulf States to northern Oklahoma; north through the eastern sections of Colorado, Wyomi ng, and Montana; and through A\"I berta, north-central Bri t ish Col umbi a and southeastern Yukon territory (Carlander 1969; Scott and Crossman 1973).</p>","language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"Twomey, K.A., Williamson, K.L., and Nelson, P.C., 1984, Habitat Suitability Index Models and Instream Flow Suitability Curves: White sucker: FWS/OBS 82/10.64, viii, 56 p.","productDescription":"viii, 56 p.","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":181767,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a81e4b07f02db649e57","contributors":{"authors":[{"text":"Twomey, Kathleen A.","contributorId":38629,"corporation":false,"usgs":true,"family":"Twomey","given":"Kathleen","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":255601,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Williamson, Kathryn L.","contributorId":50597,"corporation":false,"usgs":true,"family":"Williamson","given":"Kathryn","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":255602,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nelson, Patrick C.","contributorId":68799,"corporation":false,"usgs":true,"family":"Nelson","given":"Patrick","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":255603,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":8868,"text":"ofr84633 - 1984 - Characteristics of some silver-, and base metal-bearing, epithermal deposits of Mexico and Peru","interactions":[],"lastModifiedDate":"2018-10-22T08:50:04","indexId":"ofr84633","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1984","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":"84-633","title":"Characteristics of some silver-, and base metal-bearing, epithermal deposits of Mexico and Peru","docAbstract":"<h1>Introduction</h1>\n<p>Lithotectonic, mineralogical, and geochemical data on two silver- and base metal-bearing deposits from Peru and two from Mexico are compiled to facilitate comparisons with other epithermal deposits. Silver and base metal-bearing deposits of Mexico and Peru constitute an important portion of the world silver production derived from shallow, vein-type deposits hosted in volcanic rocks. Although these deposits are generally similar to epithermal deposits of Nevada and Colorado in the western United States, they have some important differences. Because of this, data on the geological attributes of these deposits are very useful for developing models of ore formation that can be used in mineral exploration. The data collected for this compilation are presented in the following pages in summaries of the important characteristics of each deposit. This compilation, which shows the complexities in the geology of epithermal ore deposits in Mexico and Peru, serves as a basis for further comparisons among epithermal deposits throughout the world. The case studies provide data useful to geologists and exploration!'sts interested in developing models of ore formation to be used in exploration for mineral deposits of this type. The deposits described in this report are the Guanajuato district of Guanajuato, Mexico, the Pachuca-Real del Monte district of Hidalgo, Mexico, the Colqui district of Lima, Peru, and the Julcani district of Huancavelica, Peru.</p>\n<p>Although many characteristics of the geology and geochemistry of this type of deposit were considered, the most important criterion for choosing these deposits was that they have substantial quantities of precious- and base-metal mineralization. Additional criteria for selecting the deposits were that they be hosted primarily by calc-alkaline volcanic rocks of intermediate to silicic composition and that they be younger than Tertiary in age. Many deposits in Mexico and Peru and other parts of Central and South America were excluded because the literature describing the districts is not readily available. Furthermore, many districts have not been examined in detail or the information available is of limited geological scope. The four districts that are compiled in this report were chosen because they are described in abundant literature dating from early mining reports on the general geology and mineralogy to very recent data on detailed geochemical and mineralogical studies. They were chosen as being fairly typical, classic examples of near-surface, low-temperature vein deposits as described by Lindgren (1928) in his treatise on ore deposits (Mineral deposits, McGraw-Hill, 1049 p.). These deposits are similar in aspects of their geology and geochemistry to many of the famous, epithermal silver mining districts in Colorado and Nevada including Creede, Colorado, Tonapah, Nevada, and the Sunnyside Mine of the Eureka district, Colorado, and, in the special case of Julcani, to Summitville, Colorado, and Goldfield, Nevada. The characteristics that distinguish them include overall size, production and alteration assemblage. The information documented in each summary will be used in a forthcoming series of papers on the comparative anatomy of precious and base metal deposits in North and South America.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr84633","usgsCitation":"Foley, N.K., 1984, Characteristics of some silver-, and base metal-bearing, epithermal deposits of Mexico and Peru: U.S. Geological Survey Open-File Report 84-633, 35 p., https://doi.org/10.3133/ofr84633.","productDescription":"35 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":142811,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1984/0633/report-thumb.jpg"},{"id":36439,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1984/0633/report.pdf","text":"Report","size":"471.64 KB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"Mexico, Peru","state":"Guanajuato, Hidalgo. 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