A uranium deposit discovered in 1977 in western Alaska, by means of airborne radiometric data, is the largest known in Alaska on the basis of industry reserve estimates. At about latitude 65 degrees N, it is the most northerly known sandstone-type uranium deposit in the world. The deposit lies in Eocene continental sandstone near the eastern end of the Seward Peninsula, in the southern end of a graben that extends northward into the Death Valley depositional basin.The deposit is apparently of epigenetic and supergene origin. The uranium was derived from the Cretaceous granite of the Darby pluton that forms part of the western side of Death Valley. Uranium from primary mineralization is in the subsurface in a marginal facies of the Tertiary sedimentary basin where nearshore coarse clastic rocks are interbedded with coal and lacustrine clay. Primary mineralization occurred when uranium-bearing oxidizing ground water moved downdip from the pluton eastward through transmissive clastic beds or on the surface. Uranium was deposited where the coal or other carbonaceous material produced a reducing environment in arkosic host rocks. The supergene enrichment is related to a soil horizon at the present ground surface. The most common uranium mineral is meta-autunite, but cofflnite has been identified in the primary deposits. The host rocks for the primary deposits were partly covered by basalt flows that issued from nearby vents. Some of the basalt is highly altered, and some basalt float from the supergene zone has alteration rinds that are enriched in uranium.Extensive exploratory drilling took place from 1979 to 1981. The average grade of the potential ore is 0.27 percent U 3 O 8 and the average thickness is 3 m. The calculated reserves are 1,000,000 lbs U 3 O 8 ; additional drilling would probably add to this figure.
","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.82.6.1558","issn":"00130109","usgsCitation":"Dickinson, K.A., Cunningham, K.D., and Ager, T.A., 1987, Geology and origin of the Death Valley uranium deposit, Seward Peninsula, Alaska: Economic Geology, v. 82, no. 6, p. 1558-1574, https://doi.org/10.2113/gsecongeo.82.6.1558.","productDescription":"17 p.","startPage":"1558","endPage":"1574","costCenters":[],"links":[{"id":225498,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Seward Peninsula","volume":"82","issue":"6","noUsgsAuthors":false,"publicationDate":"1987-10-01","publicationStatus":"PW","scienceBaseUri":"505a1451e4b0c8380cd549d1","contributors":{"authors":[{"text":"Dickinson, Kendell A.","contributorId":55430,"corporation":false,"usgs":true,"family":"Dickinson","given":"Kendell","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":367946,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cunningham, Kenneth D.","contributorId":99707,"corporation":false,"usgs":true,"family":"Cunningham","given":"Kenneth","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":367947,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ager, Thomas A. 0000-0002-5029-7581 tager@usgs.gov","orcid":"https://orcid.org/0000-0002-5029-7581","contributorId":736,"corporation":false,"usgs":true,"family":"Ager","given":"Thomas","email":"tager@usgs.gov","middleInitial":"A.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":367945,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014098,"text":"70014098 - 1987 - Source of lead and mineralizing brines for rossie-type Pb-Zn veins in the Frontenac axis area, New York ( USA).","interactions":[],"lastModifiedDate":"2018-10-22T08:57:53","indexId":"70014098","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Source of lead and mineralizing brines for rossie-type Pb-Zn veins in the Frontenac axis area, New York ( USA).","docAbstract":"Veins composed mainly of calcite and some galena, sphalerite, fluorite, and other minerals are widespread in the Frontenac axis area of New York and Ontario. In New York, the veins (Fig. 1) occur mainly west and northwest of Gouverneur (Brown, 1983). The veins, mined in the 1800s for lead, were first described by Emmons (1838). Smyth (1903) called these the \"Rossie lead veins,\" a name now used locally for all veins of this type. Similar veins in southeastern Ontario were described by Uglow (1916) and Sangster (1970).
\nThe steeply dipping veins are aligned along extensional fractures in metamorphic rocks of the Grenville Complex and in Paleozoic sedimentary rocks, including the Potsdam Sandstone of Late Cambrian age, and limestones as young as Middle Ordovician. However, the age of emplacement of Rossie veins is unknown. The veins are mineralogically simple, consisting of calcite (~95%) with minor and approximately equal amounts of sphalerite and galena, and sparse fluorite, barite, celestite, and chalcopyrite (Brown, 1983). Paragenetically early minerals are crushed and granulated; later undeformed minerals fill open spaces (Fig. 2). Sandstone dikes that originated from either the overlying Potsdam Sandstone or stratigraphically higher arenaceous rocks cut into the Rossie veins and occupy all available space. Their unstratified nature suggests that sand was intruded under high hydraulic pressure during tectonic events that reopened the veins. Most veins are vertical and narrow (1-3 cm wide) and those that were mined are as much as 1.7 m wide. The veins trend mainly northwest-southeast but have a local east-west orientation. The fractures and veins show evidence of strike-slip faulting with a right-lateral offset due to late reactivation of north-east-trending faults that originally formed during the Proterozoic Grenville orogeny. Relatively rare inclined veins, termed gash veins (Brown, 1983), occur in proximity to some of the regional northeast-trending faults. These veins contain open spaces lined with large, undeformed crystals of calcite (~90%) and green fluorite (~5%). The minerals of the northeast-trending gash veins, which dip to the northwest, are believed to be paragenetically late results of the same mineralization and tectonic event that produced the Rossie veins. For example, the green fluorite in the gash veins is similar in color and occurrence to small fluorite crystals in vugs in the vertical Rossie veins. Associated with the fluorite in both occurrences is coarse crystalline calcite containing tiny tetrahedra of chalcopyrite aligned along crystallographic planes.
\nThe present study of fluid inclusions and lead isotopes was done to understand better the nature and possible source of the mineralizing solutions for both vertical and gash veins and the possible origin of the lead and zinc mineralization. Large deposits of essentially syngenetic sphalerite with minor to trace galena occur in the Proterozoic rocks of this region (e.g., Balmat-Edwards, New York). Although none of these deposits are known in the immediate vicinity of Rossie veins, the possibility that Rossie veins contain remobilized metals from these older deposits was considered.
","language":"English","publisher":"Society of Economic Geologists, Inc.","doi":"10.2113/gsecongeo.82.2.489","issn":"03610128","usgsCitation":"Ayuso, R., Foley, N.K., and Brown, C.E., 1987, Source of lead and mineralizing brines for rossie-type Pb-Zn veins in the Frontenac axis area, New York ( USA).: Economic Geology, v. 82, no. 2, p. 489-491, https://doi.org/10.2113/gsecongeo.82.2.489.","productDescription":"3 p.","startPage":"489","endPage":"491","numberOfPages":"3","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":226002,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76,\n 44\n ],\n [\n -76,\n 45\n ],\n [\n -75,\n 45\n ],\n [\n -75,\n 44\n ],\n [\n -76,\n 44\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"82","issue":"2","noUsgsAuthors":false,"publicationDate":"1987-04-01","publicationStatus":"PW","scienceBaseUri":"505b9331e4b08c986b31a358","contributors":{"authors":[{"text":"Ayuso, Robert","contributorId":96350,"corporation":false,"usgs":true,"family":"Ayuso","given":"Robert","email":"","affiliations":[],"preferred":false,"id":367566,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Foley, Nora K. 0000-0003-0124-3509 nfoley@usgs.gov","orcid":"https://orcid.org/0000-0003-0124-3509","contributorId":4010,"corporation":false,"usgs":true,"family":"Foley","given":"Nora","email":"nfoley@usgs.gov","middleInitial":"K.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":367565,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Brown, C. Erwin","contributorId":96261,"corporation":false,"usgs":true,"family":"Brown","given":"C.","email":"","middleInitial":"Erwin","affiliations":[],"preferred":false,"id":367567,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014121,"text":"70014121 - 1987 - The crustal structure of the axis of the Great Valley, California, from seismic refraction measurements","interactions":[],"lastModifiedDate":"2020-05-07T15:30:26.756139","indexId":"70014121","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"The crustal structure of the axis of the Great Valley, California, from seismic refraction measurements","docAbstract":"In 1982 the U.S. Geological Survey collected six seismic refraction profiles in the Great Valley of California: three axial profiles with a maximum shot-to-receiver offset of 160 km, and three shorter profiles perpendicular to the valley axis. This paper presents the results of two-dimensional raytracing and synthetic seismogram modeling of the central axial profile. The crust of the central Great Valley is laterally heterogeneous along its axis, but generally consists of a sedimentary section overlying distinct upper, middle, and lower crustal units. The sedimentary rocks are 3-5 km thick along the profile, with velocities increasing with depth from 1.6 to 4.0 km/s. The basement (upper crust) consists of four units: 1. (1) a 1.0-1.5 km thick layer of velocity 5.4-5.8 km/s, 2. (2) a 3-4 km thick layer of velocity 6.0-6.3 km/s, 3. (3) a 1.5-3.0 km thick layer of velocity 6.5-6.6 km/s, and 4. (4) a laterally discontinuous, 1.5 km thick layer of velocity 6.8-7.0 km/s. The mid-crust lies at 11-14 km depth, is 5-8 km thick, and has a velocity of 6.6-6.7 km/s. On the northwest side of our profile the mid-crust is a low-velocity zone beneath the 6.8-7.0 km/s lid. The lower crust lies at 16-19 km depth, is 7-13 km thick, and has a velocity of 6.9-7.2 km/s. Crustal thickness increases from 26 to 29 km from NW to SE in the model. Although an unequivocal determination of crustal composition is not possible from P-wave velocities alone, our model has several geological and tectonic implications. We interpret the upper 7 km of basement on the northwest side of the profile as an ophiolitic fragment, since its thickness and velocity structure are consistent with that of oceanic crust. This fragment, which is not present 10-15 km to the west of the refraction profile, is probably at least partially responsible for the Great Valley gravity and magnetic anomalies, whose peaks lie about 10 km east of our profile. The middle and lower crust are probably gabbroic and the product of magmatic or tectonic underplating, or both. The crustal structure of the Great Valley is dissimilar to that of the adjacent Diablo Range, suggesting the existence of a fault or suture zone throughout the crust between these provinces.
","largerWorkTitle":"","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(87)90139-9","issn":"00401951","usgsCitation":"Holbrook, W., and Mooney, W.D., 1987, The crustal structure of the axis of the Great Valley, California, from seismic refraction measurements: Tectonophysics, v. 140, no. 1, p. 49-63, https://doi.org/10.1016/0040-1951(87)90139-9.","productDescription":"15 p.","startPage":"49","endPage":"63","numberOfPages":"15","costCenters":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"links":[{"id":480089,"rank":1,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1016/0040-1951(87)90139-9","text":"Publisher Index Page"},{"id":225424,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"140","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505baa71e4b08c986b322835","contributors":{"authors":[{"text":"Holbrook, W.S.","contributorId":84916,"corporation":false,"usgs":true,"family":"Holbrook","given":"W.S.","affiliations":[],"preferred":false,"id":367641,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mooney, Walter D. 0000-0002-5310-3631 mooney@usgs.gov","orcid":"https://orcid.org/0000-0002-5310-3631","contributorId":3194,"corporation":false,"usgs":true,"family":"Mooney","given":"Walter","email":"mooney@usgs.gov","middleInitial":"D.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":367640,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70015300,"text":"70015300 - 1987 - Evolution, biogeography, and systematics of Puriana: evolution and speciation in Ostracoda, III.","interactions":[],"lastModifiedDate":"2024-06-20T11:49:26.225289","indexId":"70015300","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2412,"text":"Journal of Paleontology","active":true,"publicationSubtype":{"id":10}},"title":"Evolution, biogeography, and systematics of Puriana: evolution and speciation in Ostracoda, III.","docAbstract":"Three types of geographic isolation—land barriers, deep water barriers, and climatic barriers—resulted in three distinct evolutionary responses in Neogene and Quaternary species of the epineritic ostracode genus Puriana. Through systematic, paleobiogeographic, and morphologic study of several hundred fossil and Recent populations from the eastern Pacific, western Atlantic, Gulf of Mexico, and the Caribbean, the phylogeny of the genus and the geography of speciation events were determined. Isolation of large populations by the Isthmus of Panama during the Pliocene did not lead to lineage splitting in species known to have existed before the Isthmus formed. Conversely, the establishment of small isolated populations on Caribbean islands by passive dispersal mechanisms frequently led to the evolution of new species or subspecies. Climatic changes along the southeastern United States during the Pliocene also catalyzed possible parapatric speciation as populations that immigrated to the northeastern periphery of the genus' range split to form new species. The results provide evidence that evolutionary models describing the influence of abiotic events on patterns of evolution and speciation can be tested using properly selected tectonic and climatic events and fossil groups amenable to species-level analysis. Two new species, P. bajaensis and P. paikensis, are described.
Study of the variations of direction and intensity of the geomagnetic field as recorded by the Miocene lava flows on Steens Mountain, southeastern Oregon, has resulted in a detailed description of total field behavior during a reversal in polarity. In addition to information about the polarity reversal itself, the detailed paleomagnetic record includes several thousand years of geomagnetic history preceding and following the polarity transition at 15.5 Ma. In order to test the feasibility of using this record as a means of correlation in this part of the western United States, comparisons are made of reconnaissance and previously published paleomagnetic records obtained from what has been thought to be the Steens Basalt or rocks of equivalent age. Despite the fact that many of these earlier studies were not done in detail and were not intended for correlation purposes, convincing similarities among some of the records are evident. The Steens Basalt paleomagnetic record does, indeed, have potential as a correlation tool during this time of widespread basaltic volcanism. Additionally, paleomagnetic data from flows that were sampled in detail yield a middle Miocene paleomagnetic pole at 88.3°N, 209.0° (α95 = 6.3°) for the High Lava Plains of Oregon. This pole position is statistically indistinguishable from the earth's rotational axis and implies that no tectonic rotation of this region has occurred since these lava flows were erupted. Data from selected sites within the coeval part of the Columbia River Basalt Group yield a paleomagnetic pole at 88.7°N, 171.6°E (α95 = 4.0°). The Columbia River Basalt Group pole is statistically indistinguishable from either the rotational axis or from the High Lava Plains pole. These findings indicate no post‐20 Ma differential rotation between south‐eastern Washington and south‐central Oregon, in contrast to previous interpretations.
","language":"English","publisher":"AGU","doi":"10.1029/JB092iB08p08057","issn":"01480227","usgsCitation":"Mankinen, E., Larson, E., Grommé, C., Prevot, M., and Coe, R.S., 1987, The Steens Mountain (Oregon) geomagnetic polarity transition: 3. Its regional significance: Journal of Geophysical Research B: Solid Earth, v. 92, no. B8, p. 8057-8076, https://doi.org/10.1029/JB092iB08p08057.","productDescription":"20 p.","startPage":"8057","endPage":"8076","numberOfPages":"20","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":225913,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"92","issue":"B8","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"505ba90fe4b08c986b322018","contributors":{"authors":[{"text":"Mankinen, E. A. 0000-0001-7496-2681","orcid":"https://orcid.org/0000-0001-7496-2681","contributorId":31786,"corporation":false,"usgs":true,"family":"Mankinen","given":"E. A.","affiliations":[],"preferred":false,"id":369317,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Larson, E.E.","contributorId":100508,"corporation":false,"usgs":true,"family":"Larson","given":"E.E.","email":"","affiliations":[],"preferred":false,"id":369321,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Grommé, C. S.","contributorId":38558,"corporation":false,"usgs":true,"family":"Grommé","given":"C. S.","affiliations":[],"preferred":false,"id":369318,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Prevot, M.","contributorId":75679,"corporation":false,"usgs":true,"family":"Prevot","given":"M.","email":"","affiliations":[],"preferred":false,"id":369319,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Coe, R. S.","contributorId":81228,"corporation":false,"usgs":false,"family":"Coe","given":"R.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":369320,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70014137,"text":"70014137 - 1987 - Possible Late Middle Ordovician organic carbon isotope excursion: Evidence from Ordovician oils and hydrocarbon source rocks, mid-continent and east-central United States","interactions":[],"lastModifiedDate":"2023-01-12T19:34:59.932532","indexId":"70014137","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Possible Late Middle Ordovician organic carbon isotope excursion: Evidence from Ordovician oils and hydrocarbon source rocks, mid-continent and east-central United States","docAbstract":"Oils generated by Middle Ordovician rocks are found throughout the Mid-Continent and east-central regions of the United States. Gas chromatographic characteristics of these oils include a relatively high abundance of n-alkanes with carbon numbers less than 20, a strong predominance of odd-numbered n-alkanes between C10 and C20, and relatively small amounts of branched and cyclic alkanes. Saturated and aromatic hydrocarbon fractions of 43 Ordovician oils from the Anadarko, Ardmore, Forest City, Illinois, Michigan, Salina-Sedgwick, and Williston basins and the Iowa shelf demonstrate a wide range in carbon isotope composition (^dgr13Csat = -24.9 ^pmil to -33.9 ^pmil, (^dgr13Carom = -24.3 ^pmil to -33.7 ^pmil). Saturated and aromatic hydrocarbons extracted from late Middle Ordovician shales (17 core samples) show ranges in ^dgr13C similar to that of the oils.
The wide ranges in ^dgr13C for oils and rock extracts reflect a major, positive excursion(s) (6-9 per ^pmil) in organic matter ^dgr13C in late Middle Ordovician rocks. This excursion has at least a regional significance in that it can be documented in sections 480 mi (770 km) apart in south-central Kansas and eastern Iowa. The distance may be as much as 930 mi (1,500 km) if the carbon isotope variations observed in Michigan basin Ordovician oils and in organic matter from late Middle Ordovician rocks in southwestern Ontario are related to the same carbon isotope excursion. Organic-matter ^dgr13C in core samples from south-central Kansas and eastern Iowa is not directly related to variations in quantity or quality of organic matter, or maceral compositi n. The positive excursion in organic matter ^dgr13C is a possible result of increased organic matter productivity and/or preservation.
The parallel shifts in organic and carbonate ^dgr13C in core samples from 1 E. M. Greene well, Washington County, Iowa, imply changes in the isotope composition of the ocean-atmosphere carbon reservoir. Differences in the magnitude of the carbon isotope shifts between organic matter (8.8 ^pmil) and carbonate (4.2 ^pmil) in this core suggest a decrease, either locally or regionally, in available dissolved CO2, possibly a result of high organic-matter productivity and/or limited circulation in the late Middle Ordovician seas.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/703C8074-1707-11D7-8645000102C1865D","usgsCitation":"Hatch, J.R., Jacobson, S.R., Witzke, B.J., Risatti, J., Anders, D.E., Watney, W.L., Newell, K.D., and Vuletich, A.K., 1987, Possible Late Middle Ordovician organic carbon isotope excursion: Evidence from Ordovician oils and hydrocarbon source rocks, mid-continent and east-central United States: American Association of Petroleum Geologists Bulletin, v. 71, no. 11, p. 1342-1354, https://doi.org/10.1306/703C8074-1707-11D7-8645000102C1865D.","productDescription":"13 p.","startPage":"1342","endPage":"1354","numberOfPages":"13","costCenters":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":225688,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -103.88476280424149,\n 48.772630643525844\n ],\n [\n -103.88476280424149,\n 36.63144917528669\n ],\n [\n -82.22842647308705,\n 36.63144917528669\n ],\n [\n -82.22842647308705,\n 48.772630643525844\n ],\n [\n -103.88476280424149,\n 48.772630643525844\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"71","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a7368e4b0c8380cd76ffe","contributors":{"authors":[{"text":"Hatch, Joseph R. 0000-0001-9257-0278 jrhatch@usgs.gov","orcid":"https://orcid.org/0000-0001-9257-0278","contributorId":722,"corporation":false,"usgs":true,"family":"Hatch","given":"Joseph","email":"jrhatch@usgs.gov","middleInitial":"R.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":367682,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jacobson, Stephen R.","contributorId":20086,"corporation":false,"usgs":true,"family":"Jacobson","given":"Stephen","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":367684,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Witzke, Brian J.","contributorId":40347,"corporation":false,"usgs":true,"family":"Witzke","given":"Brian","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":367687,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Risatti, J. Bruno","contributorId":28018,"corporation":false,"usgs":true,"family":"Risatti","given":"J. Bruno","affiliations":[],"preferred":false,"id":367685,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Anders, Donald E.","contributorId":35316,"corporation":false,"usgs":true,"family":"Anders","given":"Donald","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":367686,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Watney, W. Lynn","contributorId":60785,"corporation":false,"usgs":true,"family":"Watney","given":"W.","email":"","middleInitial":"Lynn","affiliations":[],"preferred":false,"id":367688,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Newell, K. David","contributorId":76074,"corporation":false,"usgs":true,"family":"Newell","given":"K.","email":"","middleInitial":"David","affiliations":[],"preferred":false,"id":367689,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Vuletich, April K.","contributorId":7430,"corporation":false,"usgs":true,"family":"Vuletich","given":"April","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":367683,"contributorType":{"id":1,"text":"Authors"},"rank":8}]}} ,{"id":70014212,"text":"70014212 - 1987 - Modeling and analysis of direct-current electrical resistivity in the Durham Triassic basin, North Carolina","interactions":[],"lastModifiedDate":"2023-11-15T16:40:43.85911","indexId":"70014212","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1761,"text":"Geoexploration","active":true,"publicationSubtype":{"id":10}},"title":"Modeling and analysis of direct-current electrical resistivity in the Durham Triassic basin, North Carolina","docAbstract":"Sixty-two Schlumberger electrical soundings were made in the Durham Triassic basin in an effort to determine basin structural geometry, depth of the sedimentary layers, and spatial distribution of individual rock facies. A digital computer program was used to invert the sounding curves of apparent resistivity versus distance to apparent resistivity versus depth. The apparent-resistivity-versus-depth data from the computer-modeling program were used to construct a geoelectric model of the basin that is believed to accurately represent the subsurface geology of the basin. The largest depth to basement in the basin along a resistivity profile (geoelectric section) was determined to be 1,800 m. A resistivity decrease was observed on certain soundings from depths of 100 to 1,000 m; below a 1,000-m depth, apparent resistivity increased to the bottom of the basin. Resistivity values for basement rocks were greater than 1,000 ohm-m and less than 350 ohm-m for the sedimentary layers in the basin. The data suggest that the basin contains a system of step faults near its eastern boundary.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7142(87)90012-3","usgsCitation":"Brown, C.E., 1987, Modeling and analysis of direct-current electrical resistivity in the Durham Triassic basin, North Carolina: Geoexploration, v. 24, no. 6, p. 429-440, https://doi.org/10.1016/0016-7142(87)90012-3.","productDescription":"12 p.","startPage":"429","endPage":"440","numberOfPages":"12","costCenters":[],"links":[{"id":225880,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"North Carolina","otherGeospatial":"Durham basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -80.11054032257658,\n 34.81424858901997\n ],\n [\n -78.71952572597303,\n 35.63369969562967\n ],\n [\n -78.29487040818577,\n 36.369481295510155\n ],\n [\n -78.80312574155963,\n 36.15648733554863\n ],\n [\n -79.43844490827757,\n 35.6255443614009\n ],\n [\n -80.1172332811392,\n 35.01166900462569\n ],\n [\n -80.28442253553915,\n 34.81424671856449\n ],\n [\n -80.11054032257658,\n 34.81424858901997\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"24","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5bd4e4b0c8380cd6f828","contributors":{"authors":[{"text":"Brown, C. Erwin","contributorId":96261,"corporation":false,"usgs":true,"family":"Brown","given":"C.","email":"","middleInitial":"Erwin","affiliations":[],"preferred":false,"id":367869,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70014754,"text":"70014754 - 1987 - Marine and nonmarine gas-bearing rocks in Upper Cretaceous Blackhawk and Neslen Formations, eastern Uinta Basin, Utah: Sedimentology, diagenesis, and source rock potential","interactions":[],"lastModifiedDate":"2023-01-17T16:02:53.961439","indexId":"70014754","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Marine and nonmarine gas-bearing rocks in Upper Cretaceous Blackhawk and Neslen Formations, eastern Uinta Basin, Utah: Sedimentology, diagenesis, and source rock potential","docAbstract":"The Upper Cretaceous Blackhawk and Neslen Formations in the eastern Uinta basin contain large amounts of thermogenic gas that was generated from interbedded humic-rich source rocks. The geometry and distribution of hydrocarbon source and reservoir rocks are controlled by depositional environment. The Blackhawk, composed of laterally extensive sandstone and locally interbedded carbonaceous siltstone and minor coal, reflects deposition in nearshore marine and backshore environments. The Neslen contains organic-rich siltstone and mudstone with lesser amounts of carbonaceous shale, coal, and lenticular sandstone that formed in coastal and lower alluvial-plain depositional settings.
Potential reservoir sandstones are composed dominantly of monocrystalline quartz grains and sedimentary lithic fragments. Mechanical compaction during early burial was followed by the precipitation of quartz, carbonate, and barite later in the burial history. Variations in porosity and permeability (2-10%; < 1 md) reflects the presence of authigenic clay, mineral cements, and dissolved lithic grains. Natural fractures, cemented with carbonate, barite, and kaolinite, occur locally.
Active hydrocarbon generation occurred in the Neslen and Blackhawk during the Oligocene and Miocene when these units were near their maximum burial depth and temperature. The rate of hydrocarbon generation decreased from the late Miocene to the present, owing to widespread cooling that occurred in response to regional uplift and erosion associated with the development of the Colorado Plateau. Temporally equivalent rocks in other areas of the basin may have experienced similar diagenetic and hydrocarbon generation histories.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/94886D4E-1704-11D7-8645000102C1865D","usgsCitation":"Pitman, J.K., Franczyk, K.J., and Anders, D.E., 1987, Marine and nonmarine gas-bearing rocks in Upper Cretaceous Blackhawk and Neslen Formations, eastern Uinta Basin, Utah: Sedimentology, diagenesis, and source rock potential: American Association of Petroleum Geologists Bulletin, v. 71, no. 1, p. 76-94, https://doi.org/10.1306/94886D4E-1704-11D7-8645000102C1865D.","productDescription":"19 p.","startPage":"76","endPage":"94","numberOfPages":"19","costCenters":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":225277,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado, Utah","otherGeospatial":"eastern Uinta basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -109.59238431596816,\n 39.387335852247276\n ],\n [\n -108.93830416597535,\n 39.798956042004676\n ],\n [\n -108.60036275514538,\n 40.174817426782084\n ],\n [\n -108.82929080764303,\n 40.28301437096778\n ],\n [\n -109.51607496513572,\n 40.45742877841448\n ],\n [\n -110.21376045846145,\n 40.47401612803404\n ],\n [\n -110.61710988429047,\n 40.291330052933034\n ],\n [\n -110.17015511512854,\n 39.89102420087448\n ],\n [\n -109.69049633846707,\n 39.437869684387124\n ],\n [\n -109.59238431596816,\n 39.387335852247276\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"71","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a51c9e4b0c8380cd6bf37","contributors":{"authors":[{"text":"Pitman, Janet K. 0000-0002-0441-779X jpitman@usgs.gov","orcid":"https://orcid.org/0000-0002-0441-779X","contributorId":767,"corporation":false,"usgs":true,"family":"Pitman","given":"Janet","email":"jpitman@usgs.gov","middleInitial":"K.","affiliations":[{"id":164,"text":"Central Energy Resources Science Center","active":true,"usgs":true},{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":369209,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Franczyk, Karen J.","contributorId":25224,"corporation":false,"usgs":true,"family":"Franczyk","given":"Karen","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":369208,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Anders, Donald E.","contributorId":35316,"corporation":false,"usgs":true,"family":"Anders","given":"Donald","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":369207,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014691,"text":"70014691 - 1987 - Trend analysis of monthly sulfur dioxide emissions in the conterminous United States, 1975-1984","interactions":[],"lastModifiedDate":"2023-02-09T17:11:23.154763","indexId":"70014691","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":924,"text":"Atmospheric Environment","active":true,"publicationSubtype":{"id":10}},"title":"Trend analysis of monthly sulfur dioxide emissions in the conterminous United States, 1975-1984","docAbstract":"Trends in monthly sulfur dioxide emissions for the 48 conterminous United States during the decade 1975-1984 are identified using a robust nonparametric procedure. Statistically significant downward trends are indicated in 32 States, upward trends appear in 10 States, and no significant trend is apparent in six States. Geographically, a distinct regional pattern of emission increases and decreases is evident with declines dominating the Eastern and Western States; increases aligning longitudinally from border to border in most of the Great Plains States, in several New England States, and in Georgia; and no trends frequently occurring in proximity to the upward trending emissions in the Plains States. A time-series decomposition of the monthly values indicates that one distinct emissions pattern commonly occurred through the period of record. This pattern is characterized by an initial emissions increase that peaks between 1977 and 1978, followed by a shallow and undulating decrease though the end of 1984. It is suggested that this signature represents the 'national' trend for the period. In addition, five regions of coherent sulfur dioxide emissions behavior are defined on the basis of seasonal occurrence of maximum and minimum emission loadings. A winter-summer, latitudinal opposition is apparent in the timing of emissions maxima, whereas an equinox-summer, longitudinal opposition is apparent in the timing of emissions minima.Trends in monthly sulfur dioxide emissions for the 48 conterminous United States during the decade 1975-1984 are identified using a robust nonparametric procedure. Statistically significant downward trends are indicated in 32 States, upward trends appear in 10 States, and no significant trend is apparent in six States. Geographically, a distinct regional pattern of emission increases and decreases is evident with declines dominating the Eastern and Western States; increases aligning longitudinally from border to border in most of the Great Plains States, in several New England States, and in Georgia; and no trends frequently occurring in proximity to the upward trending emissions in the Plains States. A time-series decomposition of the monthly values indicates that one distinct emissions pattern commonly occurred through the period of record. This pattern is characterized by an initial emissions increase that peaks between 1977 and 1978, followed by a shallow and undulating decrease through the end of 1984. It is suggested that this signature represents the 'national' trend for the period. Additional study results are discussed.","language":"English","publisher":"Elsevier","doi":"10.1016/0004-6981(87)90365-9","issn":"00046981","usgsCitation":"Lins, H., 1987, Trend analysis of monthly sulfur dioxide emissions in the conterminous United States, 1975-1984: Atmospheric Environment, v. 21, no. 11, p. 2297-2309, https://doi.org/10.1016/0004-6981(87)90365-9.","productDescription":"13 p.","startPage":"2297","endPage":"2309","costCenters":[],"links":[{"id":225271,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"21","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb7c6e4b08c986b32748d","contributors":{"authors":[{"text":"Lins, H.F.","contributorId":81508,"corporation":false,"usgs":true,"family":"Lins","given":"H.F.","affiliations":[],"preferred":false,"id":369012,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70014833,"text":"70014833 - 1987 - Character and distribution of borehole breakouts and their relationship to in situ stresses in deep Columbia River basalts","interactions":[],"lastModifiedDate":"2024-06-24T17:02:25.392229","indexId":"70014833","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":6453,"text":"Journal of Geophysical Research Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Character and distribution of borehole breakouts and their relationship to in situ stresses in deep Columbia River basalts","docAbstract":"The character and distribution of borehole breakouts in deeply buried basalts at the Hanford Site in south central Washington State are examined in light of stress indicator data and hydraulic-fracturing stress data by means of acoustic televiewer and acoustic waveform logging systems. A series of boreholes penetrating the Grande Ronde Basalt of the Columbia River Basalt Group were logged to examine the extent of breakouts at depths near 1000 m. Breakouts occur discontinuously throughout the interiors of most flows. In some boreholes the distribution of borehole wall breakouts closely correlates with the incidence of core disking. Differences in the distribution of breakouts and disking are attributed to differences in failure mechanisms. A thin interval of breakout-free basalt occurs near the upper and lower limits of flow interiors, with many intervals of breakouts terminating at the intersection of oblique fractures with the borehole. Hydraulic-fracturing stress measurement results obtained from four deep boreholes indicate anisotropic horizontal principal stresses, with maximum principal stress along an approximate north trending axis, consistent with the east trending orientation of breakouts. Acoustic waveform logs indicate that there is no measurable difference between the seismic properties of breakout-free flow tops and flow interiors. The highly coherent waveforms obtained in almost all flow interiors indicate that damage to the borehole wall associated with breakout formation remains confined to the thin annulus of stress concentration.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB092iB07p06223","issn":"01480227","usgsCitation":"Paillet, F.L., and Kim, K., 1987, Character and distribution of borehole breakouts and their relationship to in situ stresses in deep Columbia River basalts: Journal of Geophysical Research Solid Earth, v. 92, no. B7, p. 6223-6234, https://doi.org/10.1029/JB092iB07p06223.","productDescription":"12 p.","startPage":"6223","endPage":"6234","numberOfPages":"12","costCenters":[],"links":[{"id":225406,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"92","issue":"B7","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"5059f483e4b0c8380cd4bd77","contributors":{"authors":[{"text":"Paillet, Frederick L.","contributorId":63820,"corporation":false,"usgs":true,"family":"Paillet","given":"Frederick","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":369401,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kim, K.","contributorId":19303,"corporation":false,"usgs":true,"family":"Kim","given":"K.","email":"","affiliations":[],"preferred":false,"id":369400,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70014133,"text":"70014133 - 1987 - Ascaulocardium armatum (Morton 1833), new genus (Late Cretaceous): the ultimate variation on the bivalve paradigm","interactions":[],"lastModifiedDate":"2024-06-21T00:25:58.80679","indexId":"70014133","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2412,"text":"Journal of Paleontology","active":true,"publicationSubtype":{"id":10}},"title":"Ascaulocardium armatum (Morton 1833), new genus (Late Cretaceous): the ultimate variation on the bivalve paradigm","docAbstract":"Cretaceous clavagellid pelecypods are a poorly known group, and have previously received little study. Ascaulocardium armatum is conchologically the most complex burrowing pelecypod known. From the study of living clavagellids, it is possible to interpret the various tubes extending outward from the adventitious crypt of A. armatum as devices for hydraulic burrowing and deposit feeding. The conchologically complex A. armatum occurs near the beginning of the history of the Clavagellidae, and does not seem to have given rise to any younger species. Ascaulocardium armatum is known only from the Upper Cretaceous rocks (Santonian–Maastrichtian) of the east Gulf and Atlantic Coastal Plains of the United States of America, as is probably the genus Ascaulocardium. All known Cretaceous clavagellids are burrowing species having a free right valve, and this is the ancestral mode of life of the Clavagellidae. Clavagellids that have a boring habit are a more recent evolutionary development, as are burrowing species having both juvenile valves cemented to the crypt. Clavagellids probably evolved from Jurassic–Early Cretaceous pholadomyids. Almost all Cretaceous clavagellids occur outside the Tethyan Zoogeographic Realm; this distribution is in marked contrast to the modern distribution of the family. Living species mostly inhabit clear, shallow seas in subtropical to tropical shelf areas.
Lower Paleozoic carbonate rocks in the Baird Mountains quadrangle form a relatively thin, chiefly shallow-water succession that has been thrust-faulted and metamorphosed to blueschist and greenschist facies. Although this succession was thought to be mostly Devonian until recently, a large part of it is in fact pre-Silurian in age.
Middle and Upper Cambrian rocks - the first confirmed in the western Brooks Range - occur in the northeastern quarter of the quadrangle, south of Mt. Angayukaqsraq. These rocks consist of massive marble that grades upward into thin-bedded metalimestone/dolostone couplets and contain pelagiellid mollusks, acrotretid brachiopods, and agnostids. Sedimentologic features and the Pefagiellas indicate a shallow-water depositional environment. Overlying these Cambrian rocks is a thin sequence of Lower arid Middle Ordovician metalimestone and phyllite containing graptolites and cool-water, mid-shelf to basinal conodonts. Upper Ordovician rocks in the Mt. Angayukaqsraq area are bioturbated to laminated dolostone containing conodonts of warm-, shallow-water biofacies.
In the Omar and Squirrel Rivers area to the west, the Lower Ordovician carbonate rocks are thicker and quite different in lithofacies and biofacies. These rocks are mainly dolostone with locally well-developed fenestral fabric and evaporite molds, and bioturbated to laminated orange- and gray-weathering dolomitic marble and metalimestone. Conodonts and sedimentary structures indicate deposition in restricted to normal marine, shallow to very shallow water platform environments.
Exposures of Upper Silurian rocks occur near Mi. Angayukaqsraq and on the middle fork of the Squirrel River, and consist mostly of thinly laminated dolomitic mudstones. Conodonts in these rocks indicate deposition in a somewhat restricted, shallow-water environment.
Devonian carbonate rocks are widely distributed in the western Baird Mountains quadrangle; at least two distinct sequences have been identified. In the Omar and Squirrel Rivers area, Lower and Middle Devonian dolostone, metalimestone and marble are locally cherty and rich in megafossils. To the north, in the Nakolik River area, Middle and Upper Devonian marble and metalimestone are interlayered with planar- to cross-laminated quartz-carbonate metasandstone and phyllite.
Baird Mountains carbonate rocks show some striking similarities in biofacies and lithofacies to lower Paleozoic carbonate rocks of the Seward Peninsula to the southwest and the central Brooks Range to the east.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Alaskan North Slope Geology, Volumes I and II (SEPM Book 50)","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"The Pacific Section of the Society of Economic Paleontologists and Mineralogists and The Alaska geological Society","usgsCitation":"Dumoulin, J.A., and Harris, A.G., 1987, Lower Paleozoic carbonate rocks of the Baird Mountains quadrangle, western Brooks Range, Alaska, chap. of Alaskan North Slope Geology, Volumes I and II (SEPM Book 50), v. II, p. 311-336.","productDescription":"26 p.","startPage":"311","endPage":"336","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":341365,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":341364,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://archives.datapages.com/data/pac_sepm/066/066001/pdfs/311.htm"}],"country":"United States","state":"Alaska","otherGeospatial":"Baird Mountains quadrangle, Brooks Rainge","volume":"II","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"591c0fcfe4b0a7fdb43ddf1a","contributors":{"editors":[{"text":"Tailleur, Irvin L.","contributorId":105304,"corporation":false,"usgs":true,"family":"Tailleur","given":"Irvin","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":695375,"contributorType":{"id":2,"text":"Editors"},"rank":1},{"text":"Weimer, Paul","contributorId":107650,"corporation":false,"usgs":false,"family":"Weimer","given":"Paul","email":"","affiliations":[{"id":12430,"text":"University of Texas at Austin","active":true,"usgs":false}],"preferred":false,"id":695376,"contributorType":{"id":2,"text":"Editors"},"rank":2}],"authors":[{"text":"Dumoulin, Julie A. 0000-0003-1754-1287 dumoulin@usgs.gov","orcid":"https://orcid.org/0000-0003-1754-1287","contributorId":203209,"corporation":false,"usgs":true,"family":"Dumoulin","given":"Julie","email":"dumoulin@usgs.gov","middleInitial":"A.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":119,"text":"Alaska Science Center Geology Minerals","active":true,"usgs":true}],"preferred":true,"id":695373,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Harris, Anita G.","contributorId":50162,"corporation":false,"usgs":true,"family":"Harris","given":"Anita","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":695374,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":29770,"text":"wri874098 - 1987 - Effect of urbanization on the water resources of eastern Chester County, Pennsylvania","interactions":[],"lastModifiedDate":"2023-04-07T20:28:43.324863","indexId":"wri874098","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","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":"87-4098","title":"Effect of urbanization on the water resources of eastern Chester County, Pennsylvania","docAbstract":"The effects of human activity on the water resources of a 207-square-mile area of eastern Chester County was evaluated. The most serious consequence of urbanization is the contamination of ground water by volatile organic compounds, which were detected in 39 percent of the 70 wells sampled. As many as nine compounds were found in one water sample, and the concentration of total volatile organic compounds was as high as 17,400 ug/L (micrograms per liter). In the Chester Valley, volatile organic compounds are moving down the hydraulic gradient caused by quarry dewatering. Movement through the quarries reduces concentrations of these compounds and removes most of them. Phenol was detected in 28 percent of 54 wells sampled, with concentrations up to 7 ug/L.\r\n\r\n Metals, except for iron and manganese, and other trace constituents generally are not a water-quality problem. However, ground water in an area in Chester Valley has been contaminated by concentrations of boron as high as 20,000 ug/L and lithium as high as 13,000 ug/L. The ground water discharges to Valley Creek, where concentrations of boron are as high as 130 ug/L and lithium as high as 800 ug/L.\r\n\r\n Concentrations of chloride as high as 2,100 mg/L (milligrams per liter) were found in a well at a former highway salt storage site. Wells completed in carbonate rock downgradient from the Pennsylvania Turnpike had chloride concentrations as high as 350 mg/L. \r\n\r\n The base-neutral organic compounds bis(2-ethylhexyl) phthalate, di-n-butyl phthalate, and 1,2-dichlorobenzene, and the pesticides alachlor, aldrian, diazanon, DDD, DDT, dieldrin, methyl parathion, picloram, and 2,4-D were detected in a few water samples in low concentrations, However, these organic compounds do not present a widespread water-quality problem. Neither acid organic compounds nor polychlorinated napthalenes (PCN) were detected in ground water. \r\n\r\n The growth of public water and sewer systems has resulted in a significant interbasin transfer of water. Estimates for 1984 range from a net loss of 630 million gallons in the Valley Creek basin to a net gain of 783 million gallons in the Chester Creek basin. The quantity of wastewater discharged from treatment plants generally correlates well with the altitude of the water table and poorly with water use or precipitation, indicating substantial ground-water infiltration. Estimated ground-water infiltration to the West Goshen treatment plant for 1980-84 was 0.8 cubic feet per square mile, or 10 percent of the long-term average flow of Chester Creek. Estimated ground-water infiltration to the Valley Forge sewer system was as high as 4.9 million gallons per day. \r\n\r\n Dewatering operations at two active quarries in Chester Valley have lowered water levels locally and increased the range of the fluctuation of the local water table. The spread of the cones of depression caused by quarry pumping is limited by geologic and hydrologic controls. Pumping of high-capacity wells in Chester Valley has caused small local cones of depression and may have caused some reaches of Valley Creek or its tributaries to lose water. \r\n\r\n One of the greatest effects of human activity on the surface-water system has been the accumulation of organic compounds, particularly PCB and pesticides, on stream-bottom material. PCB, DDE, and dieldrin were found in bottom material from all eight streams sampled. \r\n\r\n Land-use changes in 10 selected subbasins were quantified and related to stream-benthic invertebrate diversity index. from 1970-80, the diversity index increased at all sites. Subbasins that had a greater change in land use had a greater increase in diversity index. The increase may be due to the banning of certain pesticides such as DDT, a decreasing use of pesticides in urbanizing subbasins, or flushing or burial of older pesticide-contaminated sediment.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874098","usgsCitation":"Sloto, R., 1987, Effect of urbanization on the water resources of eastern Chester County, Pennsylvania: U.S. Geological Survey Water-Resources Investigations Report 87-4098, Report: viii, 131 p.; 2 Plates: 36.43 x 35.29 inches and 29.23 x 18.83 inches, https://doi.org/10.3133/wri874098.","productDescription":"Report: viii, 131 p.; 2 Plates: 36.43 x 35.29 inches and 29.23 x 18.83 inches","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":415467,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_46767.htm","linkFileType":{"id":5,"text":"html"}},{"id":58569,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4098/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":58570,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4098/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":58568,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4098/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124903,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4098/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","county":"Chester County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -75.2917,\n 40.243\n ],\n [\n -75.8667,\n 40.243\n ],\n [\n -75.8667,\n 39.9\n ],\n [\n -75.2917,\n 39.9\n ],\n [\n -75.2917,\n 40.243\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4be4b07f02db62542f","contributors":{"authors":[{"text":"Sloto, R. A.","contributorId":36155,"corporation":false,"usgs":true,"family":"Sloto","given":"R. A.","affiliations":[],"preferred":false,"id":202093,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":21461,"text":"ofr86247 - 1987 - Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon","interactions":[{"subject":{"id":21461,"text":"ofr86247 - 1987 - Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon","indexId":"ofr86247","publicationYear":"1987","noYear":false,"title":"Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon"},"predicate":"SUPERSEDED_BY","object":{"id":38449,"text":"pp1408D - 1988 - Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon","indexId":"pp1408D","publicationYear":"1988","noYear":false,"chapter":"D","title":"Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon"},"id":1}],"supersededBy":{"id":38449,"text":"pp1408D - 1988 - Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon","indexId":"pp1408D","publicationYear":"1988","noYear":false,"title":"Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon"},"lastModifiedDate":"2023-02-21T13:57:21.054086","indexId":"ofr86247","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","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":"86-247","title":"Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon","docAbstract":"Three geochemical methods were used to determine chemical reactions that control solute concentrations in the Snake River Plain regional aquifer system: (1) Calculation of a regional solute balance within the aquifer and of mineralogy in the aquifer framework to identify solute reactions, (2) comparison of thermodynamic mineral saturation indices with plausible solute reactions, and (3) comparison of stable-isotope ratios of the ground water with those in the aquifer framework. The geothermal ground-water system underlying the main aquifer system was examined by calculating thermodynamic mineral saturation indices, stable-isotope ratios of geothermal water, geothermometry, and radiocarbon dating.
Water budgets, hydrologic arguments, and isotopic analyses for the eastern Snake River Plain aquifer system demonstrate that most, if not all, water is of local meteoric and not juvenile or formation origin. Solute-balance, isotopic, mineralogic, and thermodynamic arguments suggest that about 20 percent of the solutes are derived from reactions with rocks forming the aquifer framework.
Solute reactions indicate that calcite and silica are precipitated in the aquifer. Mineralogic evidence and thermodynamic arguments suggest that olivine, pyroxene, pyrite, and anhydrite are being dissolved and plagioclase is being weathered. Large amounts of sodium and chloride, relative to their concentration in the igneous rock, are being removed from the aquifer. Release of fluids from inclusions in the igneous rocks, and initial flushing of grain boundaries and pores of detrital marine sediments in interbeds are believed to be the source of the sodium chloride. Identification and quantification of reactions controlling solute concentrations in ground water in the eastern plain indicate that the aquifer is not a large mixing vessel that simply stores and transmits water and solutes but is undergoing diagenesis and is both a source and sink for solutes.
Evaluation of solute concentrations and stable-isotope ratios of hydrogen, oxygen, carbon, and sulfur along ground-water flowpaths that transect irrigated areas suggests that irrigation water may have altered solute concentrations and isotope ratios in the eastern Snake River Plain aquifer system. The changes, however, have been small, owing to similarity of solute concentrations in applied irrigation water and in native ground water and rapid movement and large dispersivity of the aquifer.
Reactions controlling solutes in the western Snake River basin are believed to be similar to those in the eastern basin but, because of different hydrologic conditions, a definitive analysis could not be made.
The regional geothermal system that underlies the Snake River Plain contains total dissolved solids similar to those in the overlying Snake River Plain aquifer system but contains higher concentrations of sodium, bicarbonate, silica, fluoride, sulfate, chloride, arsenic, boron, and lithium, and lower concentrations of calcium, magnesium, and hydrogen. These solutes are believed to be derived from reactions similar to those in the Snake River Plain aquifer system, except that ion exchange may be a significant mechanism controlling solute concentrations in the geothermal system.
Geothermometry calculations of selected ground-water samples from known geothermal areas throughout the basin suggest that the geothermal system is large in areal extent but has relatively low temperatures. Approximately half of the silica-quartz calculated water temperatures are greater than 90 degrees Celsius. Radiocarbon dating of geothermal water in the Salmon Falls and Bruneau-Grand View areas in the south-central part of the Snake River basin suggests that residence time of the geothermal water is about 17,700 years.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr86247","collaboration":"A contribution of the Regional Aquifer-System Analysis program","usgsCitation":"Wood, W.W., and Low, W.H., 1987, Solute geochemistry of the Snake River plain regional aquifer system, Idaho and eastern Oregon: U.S. Geological Survey Open-File Report 86-247, xi, 146 p., https://doi.org/10.3133/ofr86247.","productDescription":"xi, 146 p.","costCenters":[],"links":[{"id":154007,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1986/0247/report-thumb.jpg"},{"id":382936,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1986/0247/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho, Oregon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.04833984375001,\n 42.06560675405716\n ],\n [\n -111.15966796875,\n 42.06560675405716\n ],\n [\n -111.15966796875,\n 48.951366470947725\n ],\n [\n -117.04833984375001,\n 48.951366470947725\n ],\n [\n -117.04833984375001,\n 42.06560675405716\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e479de4b07f02db491f0a","contributors":{"authors":[{"text":"Wood, Warren W.","contributorId":213538,"corporation":false,"usgs":false,"family":"Wood","given":"Warren","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":184469,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Low, Walton H.","contributorId":92672,"corporation":false,"usgs":true,"family":"Low","given":"Walton","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":184470,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":29124,"text":"wri874015 - 1987 - Ground-water flow and shallow-aquifer properties in the Rio Grande inner valley south of Albuquerque, Bernalillo County, New Mexico","interactions":[],"lastModifiedDate":"2023-04-11T20:27:18.117104","indexId":"wri874015","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","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":"87-4015","title":"Ground-water flow and shallow-aquifer properties in the Rio Grande inner valley south of Albuquerque, Bernalillo County, New Mexico","docAbstract":"The purpose of this investigation was to describe the water table configuration and its temporal variations, estimate aquifer properties, and evaluate the interaction of groundwater and surface water in the inner valley of the Rio Grande in southern Albuquerque, New Mexico, where groundwater contamination is a continuing concern. The upper 150 ft of sedimentary deposits in the inner valley, mostly alluvium that consists of cobbles, gravel, sand, silt, and clay, was emphasized because of its susceptibility to contamination. A map of the water table on February 28, 1986 shows that flow generally is parallel to the river and the gradient is approximately 5 ft/mi or 0.0001. In areas affected by municipal and industrial groundwater withdrawals, declines may exceed 10 ft, and the water table gradient is as much as 20 ft/mi or 0.004. The gradient also is steeper near drains, particularly during the irrigation season. In the area east of the community of Mountainview the direction of water movement may have reversed between 1936 and 1986; flow near appears to be toward the east or southeast. Groups of four piezometers, each screened at a different depth, were monitored to describe seasonal changes of the water table. Vertical gradients between piezometers ranged from 0.014 upward to 0.047 downward from July 1985 to June 1986, but were downward most of the year, particulary during the irrigation season. The horizontal hydraulic conductivity of a 15-ft-thick clay and silt bed beneath Rio Bravo Boulevard is estimated to be 0.0001 ft/day. The average interstitial velocity down through this bed is estimated to range from about 0.0002 to 0.0005 ft/day. The fluctuations of the water table at the piezometers nearest the Rio Grande do not appear to be affected by the riverside drain.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874015","usgsCitation":"Peter, K.D., 1987, Ground-water flow and shallow-aquifer properties in the Rio Grande inner valley south of Albuquerque, Bernalillo County, New Mexico: U.S. Geological Survey Water-Resources Investigations Report 87-4015, iv, 29 p., https://doi.org/10.3133/wri874015.","productDescription":"iv, 29 p.","costCenters":[],"links":[{"id":57994,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4015/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123690,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4015/report-thumb.jpg"},{"id":415599,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_46703.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"New Mexico","county":"Bernalillo County","city":"Albuquerque","otherGeospatial":"Rio Grande Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -106.5833,\n 35.095\n ],\n [\n -106.7292,\n 35.095\n ],\n [\n -106.7292,\n 34.9394\n ],\n [\n -106.5833,\n 34.9394\n ],\n [\n -106.5833,\n 35.095\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66cd65","contributors":{"authors":[{"text":"Peter, K. D.","contributorId":94319,"corporation":false,"usgs":true,"family":"Peter","given":"K.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":200984,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":30512,"text":"wri874153 - 1987 - Ground-water withdrawals and changes in ground-water levels, ground-water quality, and land-surface subsidence in the Houston district, Texas, 1980-84","interactions":[],"lastModifiedDate":"2023-06-07T21:28:49.437566","indexId":"wri874153","displayToPublicDate":"1987-01-01T00:00:00","publicationYear":"1987","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":"87-4153","title":"Ground-water withdrawals and changes in ground-water levels, ground-water quality, and land-surface subsidence in the Houston district, Texas, 1980-84","docAbstract":"During 1980-84, ground-water withdrawals from the Chicot and Evangeline aquifers in the Houston district decreased from 511 million gallons per day to 444 million gallons per day. This 13-percent decrease was due to the increased availability of surface water and a decreased demand for water. The largest decreases in ground-water withdrawals occurred in the Houston area. Ground-water pumpage was 219.2 million gallons per day during 1984 compared to 254.8 million gallons per day during 1980. Decreases in ground-water withdrawals from 1980 through 1984 occurred in most of the other areas in the Houston district (Pasadena, Katy, Baytown-LaPorte, and Texas City). Large decreases in ground-water withdrawals for rice irrigation in the Katy area were offset by increases in ground-water withdrawals for public supply. Hence, in the Katy area, the quantity of ground water withdrawn during 1984, 148.9 million gallons per day, was only slightly less than the 157.5 million gallons per day withdrawn during 1980.
Water levels generally rose in the eastern part of the Houston district and declined in the western part from spring 1980 to spring 1985. The rise of water levels in wells in the Chicot and Evangeline aquifers was as much as 80 feet and 60 feet, respectively. The decline of water levels in wells in the Chicot and Evangeline aquifers was as much as 40 feet and 80 feet, respectively.
Slight decreases in chloride concentrations in water from the Chicot aquifer occurred in the Alta Loma area between 1980 and 1984. In 1980, chloride concentrations in water from the Chicot aquifer ranged from 250 to 790 milligrams per liter, whereas in 1984, chloride concentrations ranged from 180 to 710 milligrams per liter. Water from one well in the Texas City area had an increase in chloride concentrations from 265 milligrams per liter in 1980 to 300 milligrams per liter in 1984. In water from another well in the Texas City area, chloride concentrations decreased from 760 milligrams per liter in 1980 to 710 milligrams per liter in 1984. The concentrations of chloride and dissolved solids in water from the Evangeline aquifer remained less than 100 milligrams per liter and 500 milligrams per liter during 1980-84.
Land-surface subsidence is still evident in the Houston district. Subsidence rates between 1980 and early 1985 in the eastern and southeastern parts of the Houston district were less than during 1975-79. At the Seabrook site, where a monitor measures most of the subsidence, the average compaction rate during 1980 to early 1985 was 0.04 foot per year while during 1975-79, the rate was 0.14 foot per year. However, subsidence rates in the western, southwestern, and northern parts of the Houston district during 1980 to early 1985 increased from the 1975-79 rates. At the Addicks site, the land surface has subsided at a rate of about 0.17 foot per year from 1980 to early 1985. The subsidence rate from 1975 through 1979 at the site was 0.11 foot per year.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri874153","collaboration":"Prepared in cooperation with the City of Houston and the Harris-Galveston Coastal Subsidence District","usgsCitation":"Williams, J.F., and Ranzau, C., 1987, Ground-water withdrawals and changes in ground-water levels, ground-water quality, and land-surface subsidence in the Houston district, Texas, 1980-84: U.S. Geological Survey Water-Resources Investigations Report 87-4153, Report: v, 56 p.; 4 Plates:18.40 x 12.66 inches or smaller, https://doi.org/10.3133/wri874153.","productDescription":"Report: v, 56 p.; 4 Plates:18.40 x 12.66 inches or smaller","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":59288,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4153/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59287,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4153/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":59286,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4153/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":403224,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1987/4153/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":124304,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1987/4153/report-thumb.jpg"},{"id":110245,"rank":7,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_46815.htm","linkFileType":{"id":5,"text":"html"}},{"id":59289,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1987/4153/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Texas","city":"Houston","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -96.06170654296875,\n 29.44438130948883\n ],\n [\n -94.910888671875,\n 29.44438130948883\n ],\n [\n -94.910888671875,\n 30.306503259848835\n ],\n [\n -96.06170654296875,\n 30.306503259848835\n ],\n [\n -96.06170654296875,\n 29.44438130948883\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db69662f","contributors":{"authors":[{"text":"Williams, James F. III","contributorId":173660,"corporation":false,"usgs":false,"family":"Williams","given":"James","suffix":"III","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":203379,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ranzau, C.E. Jr.","contributorId":41831,"corporation":false,"usgs":true,"family":"Ranzau","given":"C.E.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":203378,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":27111,"text":"wri854231 - 1986 - Hydrogeologic conditions and saline-water intrusion, Cape Coral, Florida, 1978-81","interactions":[],"lastModifiedDate":"2021-12-13T12:10:47.311118","indexId":"wri854231","displayToPublicDate":"2021-12-12T20:30:00","publicationYear":"1986","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":"85-4231","title":"Hydrogeologic conditions and saline-water intrusion, Cape Coral, Florida, 1978-81","docAbstract":"The upper limestone unit of the intermediate aquifer system, locally called the upper Hawthorn aquifer, is the principal source of freshwater for Cape Coral, Florida. The aquifer has been contaminated with saline water by downward intrusion from the surficial aquifer system and by upward intrusion from the Floridan aquifer system. Much of the intrusion has occurred through open wellbores where steel casings are short or where casings have collapsed because of corrosion. Saline-water contamination of the upper limestone unit due to downward intrusion from the surficial aquifer is most severe in the southern and eastern parts of Cape Coral; contamination due to upward intrusion has occurred in many areas throughout Cape Coral. Intrusion is amplified in areas of heavy water withdrawals and large water-level declines. (USGS)","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri854231","collaboration":"Prepared in cooperation with the City of Cape Coral","usgsCitation":"Fitzpatrick, D., 1986, Hydrogeologic conditions and saline-water intrusion, Cape Coral, Florida, 1978-81: U.S. Geological Survey Water-Resources Investigations Report 85-4231, iv, 31 p., https://doi.org/10.3133/wri854231.","productDescription":"iv, 31 p.","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":124482,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1985/4231/coverthb.jpg"},{"id":55970,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1985/4231/wri854231.pdf","text":"Report","size":"1.67 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 85-4231"}],"country":"United States","state":"Florida","city":"Cape Coral","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -82.11456298828124,\n 26.474260922876063\n ],\n [\n -81.81243896484375,\n 26.474260922876063\n ],\n [\n -81.81243896484375,\n 26.79588031886341\n ],\n [\n -82.11456298828124,\n 26.79588031886341\n ],\n [\n -82.11456298828124,\n 26.474260922876063\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
The origins of paleoflood hydrology in the United States can be traced back to the beginning of the 19th century, when windgaps and watergaps in the Applachians were believed to have been eroded by extraordinary floods as large lakes that were ponded behind the ridges rapidly drained. Sediment evidence for extraordinary floods was evoked several decades later when glacial sediments in New England were interpreted as deposits from the great Biblical deluge, and estimates of the depth and velocity of the great flood were attempted. The popularization of the glacial origins of drift by Agassiz by 1840 resulted in strong beliefs in uniformitarianism and waning interests in paleoflood investigations. The documentation of the origins of the channeled scablands in eastern Washington by catastrophic glacial outbreak floods, begun by Bretz in the early 1920s, led to renewed interest in paleoflood hydrology. Subsequent efforts to reconstruct hydraulic variables of past floods used conventional open channel flow equations applied to other enormous Pleistocene floods. The elevation of sediments was used as a paleostage estimator in the 1880s, and botanical techniques for estimating paleoflood frequency and magnitude were well documented by the mid-1960s. Since 1970, an exponential expansion has occurred in the recognition and use of paleoflood hydrology in the United States.
","language":"English","publisher":"American Geophysical Union","publisherLocation":"Washington, D.C.","doi":"10.1029/EO067i017p00425-02","usgsCitation":"Costa, J.E., 1986, A history of paleoflood hydrology in the United States: Eos, Earth and Space Science News, v. 67, no. 17, p. 425-430, https://doi.org/10.1029/EO067i017p00425-02.","productDescription":"4 p.","startPage":"425","endPage":"430","numberOfPages":"4","temporalStart":"1800-01-01","temporalEnd":"1970-12-31","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true},{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":328641,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"67","issue":"17","noUsgsAuthors":false,"publicationDate":"2011-06-03","publicationStatus":"PW","scienceBaseUri":"57da74ade4b090824ffb7e0b","contributors":{"authors":[{"text":"Costa, John E.","contributorId":105743,"corporation":false,"usgs":true,"family":"Costa","given":"John","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":648798,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70157450,"text":"70157450 - 1986 - Hydrogeology and ground-water use and quality, Brown County, Wisconsin","interactions":[],"lastModifiedDate":"2018-01-08T19:27:03","indexId":"70157450","displayToPublicDate":"2015-04-06T04:30:00","publicationYear":"1986","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5596,"text":"Wisconsin Geological & Natural History Survey Information Circular","active":true,"publicationSubtype":{"id":2}},"seriesNumber":"57","title":"Hydrogeology and ground-water use and quality, Brown County, Wisconsin","docAbstract":"The Paleozoic rock of Brown County includes formations of Cambrian, Ordovician, and Silurian age. These formations are eastward-dipping sedimentary rock that rest on Precambrian crystalline rock and are overlain by Pleistocene deposits. The units that are the principal sources of ground water were grouped into three aquifers (upper, St. Peter, and Elk Mound), and the less permeable units are grouped into three confining units (Maquoketa-Sinnipee, St. Lawrence, and Precambrian). The geologic and hydraulic characteristics of the aquifers and confining units are estimated from logs of more than 1,000 Brown County wells, from results of a packer test, and from published values.
\nRecharge to the water table, which was estimated at five monitored sites, ranges from 1 to 6 inches a year; most recharge is contributed by spring snowmelt and rainfall. A cone of depression caused by pumping the deeper aquifers in the Green Bay metropolitan area induces flow from the upper aquifer to the underlying st. Peter aquifer throughout most of the county. Several reaches of Duck Creek and the Suamico River also contribute water to the aquifers. A
\nbout 13 million gallons per day of ground water was pumped in Brown County during 1979, 63 percent of which was from wells open to both the St. Peter and Elk Mound aquifers. Municipal and industrial water users pumped 9.44 million gallons per day or 72 percent of the ground water withdrawn in 1979.
\nMost ground :water in the county is a calcium magnesium bicarbonate type. However, water from wells sampled in an area between the Fox River and Silurian escarpment have elevated levels of sodium (44 milligrams per liter) and sulfate (226 milligrams per liter). Water from wells that tap rocks older than Silurian dolomite contains high concentrations of strontium (more than 2.4 milligrams per liter) and fluoride (more than 0.85 milligrams per liter).
\nA three-dimensional digital model was used to simulate flow in the ground-water system. Model results indicate that sources of ground water pumped from wells tapping the St. Peter and Elk Mound aquifers in Brown County, 1979, include 4.8 million gallons per day of underflow, most of which enters the county across the west border; 1.9 million gallons per day of flow from vertical leakage within the county; and 1.5 million gallons per day from storage. The model is most sensitive to the horizontal hydraulic conductivity of the upper aquifer. Vertical hydraulic conductivity of the confining units and recharge rates to the water-table aquifer are the least well-defined model parameters.
","language":"English","publisher":"Wisconsin Geological & Natural History Survey","collaboration":"In cooperation with the University of Wisconsin-Extension, Geological and Natural History Survey","usgsCitation":"Krohelski, J.T., and Brown, B., 1986, Hydrogeology and ground-water use and quality, Brown County, Wisconsin: Wisconsin Geological & Natural History Survey Information Circular 57, v, 42 p.","productDescription":"v, 42 p.","numberOfPages":"49","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":308459,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":350385,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://wgnhs.uwex.edu/pubs/download_ic57/"}],"country":"United States","state":"Wisconsin","county":"Brown County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-87.9887,44.6778],[-87.9888,44.6728],[-87.9901,44.6719],[-87.9907,44.6719],[-87.9914,44.6719],[-87.9932,44.6751],[-87.9939,44.6751],[-87.9952,44.6751],[-87.9958,44.6747],[-87.9971,44.6719],[-87.9991,44.672],[-88.0029,44.6738],[-88.0061,44.6743],[-88.0067,44.6739],[-88.0074,44.6734],[-88.008,44.673],[-88.0074,44.6716],[-88.0062,44.6702],[-88.0005,44.6679],[-87.9998,44.6674],[-87.9998,44.6665],[-88.0005,44.6651],[-88.0012,44.6647],[-88.0018,44.6647],[-88.0075,44.6679],[-88.0082,44.6679],[-88.0088,44.6675],[-88.0082,44.6638],[-88.009,44.6575],[-88.0099,44.6461],[-88.0106,44.6456],[-88.0112,44.6456],[-88.0144,44.6466],[-88.0151,44.6466],[-88.0151,44.6457],[-88.0145,44.6429],[-88.0145,44.642],[-88.0191,44.6352],[-88.0185,44.6343],[-88.0153,44.6338],[-88.0147,44.6334],[-88.0117,44.6251],[-88.0074,44.6141],[-88.0068,44.6132],[-88.0004,44.6118],[-87.9941,44.6067],[-87.9816,44.5947],[-87.9797,44.5933],[-87.979,44.5924],[-87.9798,44.5878],[-87.9805,44.5828],[-87.9818,44.5824],[-87.983,44.5892],[-87.9848,44.591],[-87.9861,44.5943],[-87.9898,44.6002],[-88.0012,44.6077],[-88.0082,44.61],[-88.0088,44.61],[-88.0101,44.61],[-88.0107,44.6105],[-88.0107,44.6119],[-88.0136,44.6228],[-88.0149,44.6238],[-88.0155,44.6247],[-88.0162,44.6247],[-88.0168,44.6247],[-88.0175,44.6234],[-88.0182,44.6188],[-88.0178,44.6092],[-88.0187,44.5974],[-88.0188,44.5946],[-88.0207,44.5937],[-88.0214,44.5924],[-88.0214,44.5901],[-88.019,44.585],[-88.0204,44.5782],[-88.0191,44.5782],[-88.0185,44.5759],[-88.0173,44.5745],[-88.0179,44.5732],[-88.0192,44.5723],[-88.0211,44.5737],[-88.0217,44.5755],[-88.0237,44.5755],[-88.0269,44.5746],[-88.0365,44.577],[-88.039,44.5766],[-88.0462,44.5726],[-88.0468,44.5717],[-88.0475,44.5694],[-88.0476,44.5658],[-88.0451,44.5644],[-88.0425,44.5639],[-88.0406,44.5648],[-88.0399,44.5675],[-88.0386,44.5684],[-88.0335,44.5665],[-88.0284,44.5637],[-88.0259,44.5614],[-88.0234,44.56],[-88.0234,44.5591],[-88.0247,44.5582],[-88.0266,44.5573],[-88.0286,44.5569],[-88.0337,44.5583],[-88.0349,44.5583],[-88.0356,44.5574],[-88.0356,44.5565],[-88.0287,44.5514],[-88.0255,44.5495],[-88.0249,44.5486],[-88.0249,44.5477],[-88.0249,44.5463],[-88.0218,44.5445],[-88.0212,44.5436],[-88.0212,44.5427],[-88.0218,44.5422],[-88.027,44.5391],[-88.0264,44.5386],[-88.0245,44.5386],[-88.0226,44.5386],[-88.02,44.5399],[-88.018,44.5435],[-88.0167,44.544],[-88.0154,44.5435],[-88.0142,44.5417],[-88.0116,44.5407],[-88.0046,44.5393],[-87.9925,44.5337],[-87.9811,44.5303],[-87.9664,44.5284],[-87.9504,44.5277],[-87.9401,44.529],[-87.9343,44.5316],[-87.931,44.5348],[-87.927,44.5416],[-87.9244,44.5429],[-87.9171,44.5529],[-87.9105,44.5605],[-87.9079,44.5628],[-87.9053,44.5664],[-87.9052,44.5682],[-87.9045,44.571],[-87.9031,44.575],[-87.905,44.5755],[-87.9095,44.576],[-87.914,44.5743],[-87.916,44.5743],[-87.9172,44.5752],[-87.9172,44.5761],[-87.9094,44.5797],[-87.9036,44.5819],[-87.8964,44.5864],[-87.8918,44.5918],[-87.886,44.5963],[-87.8839,44.6026],[-87.8813,44.6049],[-87.8741,44.6085],[-87.8695,44.6139],[-87.861,44.6188],[-87.8585,44.6192],[-87.8565,44.6187],[-87.8527,44.6178],[-87.8495,44.6173],[-87.8463,44.6177],[-87.8262,44.6284],[-87.8177,44.6338],[-87.8131,44.636],[-87.806,44.6373],[-87.7919,44.638],[-87.7823,44.6374],[-87.7732,44.6396],[-87.7706,44.6414],[-87.7654,44.645],[-87.7628,44.6477],[-87.7643,44.5888],[-87.7646,44.5017],[-87.7655,44.4146],[-87.7665,44.3271],[-87.8879,44.3277],[-87.888,44.2402],[-87.9238,44.2402],[-88.0099,44.2407],[-88.0431,44.2411],[-88.1317,44.2411],[-88.163,44.2414],[-88.193,44.2421],[-88.1919,44.3288],[-88.1921,44.3871],[-88.1921,44.4167],[-88.1918,44.5016],[-88.1908,44.5864],[-88.2203,44.5858],[-88.2453,44.5846],[-88.2446,44.6239],[-88.2432,44.664],[-88.2528,44.6641],[-88.2525,44.6846],[-88.2435,44.6845],[-88.2287,44.6844],[-88.2289,44.6725],[-88.1833,44.6734],[-88.1312,44.677],[-88.0092,44.6775],[-87.9887,44.6778]]]},\"properties\":{\"name\":\"Brown\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5603cd44e4b03bc34f544b0e","contributors":{"authors":[{"text":"Krohelski, J. T.","contributorId":59046,"corporation":false,"usgs":true,"family":"Krohelski","given":"J.","email":"","middleInitial":"T.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":573205,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brown, B.A.","contributorId":147913,"corporation":false,"usgs":false,"family":"Brown","given":"B.A.","email":"","affiliations":[],"preferred":false,"id":573206,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70044030,"text":"70044030 - 1986 - Water resources of the Park City area, Utah, with emphasis on ground water","interactions":[{"subject":{"id":14181,"text":"ofr85638 - 1985 - Water resources of the Park City area, Utah, with emphasis on ground water","indexId":"ofr85638","publicationYear":"1985","noYear":false,"title":"Water resources of the Park City area, Utah, with emphasis on ground water"},"predicate":"SUPERSEDED_BY","object":{"id":70044030,"text":"70044030 - 1986 - Water resources of the Park City area, Utah, with emphasis on ground water","indexId":"70044030","publicationYear":"1986","noYear":false,"title":"Water resources of the Park City area, Utah, with emphasis on ground water"},"id":1}],"lastModifiedDate":"2016-12-13T09:32:51","indexId":"70044030","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1986","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":294,"text":"Technical Publication","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"85","title":"Water resources of the Park City area, Utah, with emphasis on ground water","docAbstract":"The Park City area is a rapidly growing residential and recreational area about 30 miles east of Sal t Lake City (fig. 1). The area of study is about 140 square miles in which the principle industries are agriculture, skiing, and other recreational activities. The area once was a major lead- and silver-mining district, but no mines were active in 1984. A resumption in mining activity, however, could take place with an increase in the price of metals.
The population of the Park City area is expected to increase rapidly in the near future; and the provision of an adequate water supply for the growing population, while avoiding harmful affects of development, is a major concern for local municipalities, developers, and the Utah Division of Water Rights. In addition, agricultural interests in and below the area are concerned about the effects of increased ground-water withdrawals on streamflow, which is fully appropriated by downstream users. The area also contains the proposed site for the Jordanelle dam, a part of the Bonneville unit of the central Utah Project. The damsite is near an historic mining area; and mining companies are concerned that if mining is resumed, the reservoir may create some additional dewatering problems in the mines.
","language":"English","publisher":"Utah Department of Natural Resources, Division of Water Rights","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared by the United States Geological Survey in cooperation with the Utah Department of Natural Resources, Division of Water Rights","usgsCitation":"Holmes, W.F., Thompson, K.R., and Enright, M., 1986, Water resources of the Park City area, Utah, with emphasis on ground water: Technical Publication 85, vi, 82 p.","productDescription":"vi, 82 p.","numberOfPages":"90","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":268267,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268266,"type":{"id":11,"text":"Document"},"url":"https://waterrights.utah.gov/docSys/v920/w920/w92000aa.pdf"},{"id":332012,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://www.waterrights.utah.gov/cgi-bin/libview.exe?Modinfo=Viewpub&LIBNUM=20-6-170"}],"country":"United States","state":"Utah","city":"Park City","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.8792724609375,\n 40.44694705960048\n ],\n [\n -111.8792724609375,\n 41.025499378313754\n ],\n [\n -111.1376953125,\n 41.025499378313754\n ],\n [\n -111.1376953125,\n 40.44694705960048\n ],\n [\n -111.8792724609375,\n 40.44694705960048\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"512c9623e4b0855fde669820","contributors":{"authors":[{"text":"Holmes, Walter F.","contributorId":31737,"corporation":false,"usgs":true,"family":"Holmes","given":"Walter","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":474673,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Thompson, Kendall R.","contributorId":100854,"corporation":false,"usgs":true,"family":"Thompson","given":"Kendall","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":474675,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Enright, Michael","contributorId":99979,"corporation":false,"usgs":true,"family":"Enright","given":"Michael","email":"","affiliations":[],"preferred":false,"id":474674,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70044324,"text":"70044324 - 1986 - Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole Counties, Oklahoma","interactions":[{"subject":{"id":20205,"text":"ofr84445 - 1984 - Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole counties, Oklahoma","indexId":"ofr84445","publicationYear":"1984","noYear":false,"title":"Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole counties, Oklahoma"},"predicate":"SUPERSEDED_BY","object":{"id":70044324,"text":"70044324 - 1986 - Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole Counties, Oklahoma","indexId":"70044324","publicationYear":"1986","noYear":false,"title":"Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole Counties, Oklahoma"},"id":1}],"lastModifiedDate":"2013-03-02T14:44:35","indexId":"70044324","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1986","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":244,"text":"Circular","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"89","title":"Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole Counties, Oklahoma","docAbstract":"A study of water-quality degradation due to brine contamination was made in an area of ~1,700 mi2 in east-central Oklahoma. The study area coincides in part with the outcrop of the Vamoosa-Ada aquifer of Pennsylvanian age.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","collaboration":"Prepared by the United States Geological Survey in cooperation with the Oklahoma Geological Survey","usgsCitation":"Morton, R.B., 1986, Effects of brine on the chemical quality of water in parts of Creek, Lincoln, Okfuskee, Payne, Pottawatomie, and Seminole Counties, Oklahoma: Circular 89, iii, 38 p.; Map: 1 Sheet.","productDescription":"iii, 38 p.; Map: 1 Sheet","startPage":"i","endPage":"38","numberOfPages":"42","costCenters":[{"id":516,"text":"Oklahoma Water Science Center","active":true,"usgs":true}],"links":[{"id":268663,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268661,"type":{"id":11,"text":"Document"},"url":"https://www.ogs.ou.edu/pubsscanned/Circulars/circular89mm.pdf"},{"id":268662,"type":{"id":17,"text":"Plate"},"url":"https://www.ogs.ou.edu/pubsscanned/CircularsPlates/C89P1.pdf"}],"country":"United States","state":"Oklahoma","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0,33.62 ], [ -103.0,37.0 ], [ -94.43,37.0 ], [ -94.43,33.62 ], [ -103.0,33.62 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51332d74e4b0c316aaf0681d","contributors":{"authors":[{"text":"Morton, Robert B.","contributorId":50899,"corporation":false,"usgs":true,"family":"Morton","given":"Robert","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":475292,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70046142,"text":"70046142 - 1986 - Geohydrology of the Vamoosa-Ada aquifer east-central Oklahoma with a section on chemical quality of water","interactions":[{"subject":{"id":8675,"text":"ofr77487 - 1977 - Hydrologic data for the Vamoosa Aquifer, east-central Oklahoma","indexId":"ofr77487","publicationYear":"1977","noYear":false,"title":"Hydrologic data for the Vamoosa Aquifer, east-central Oklahoma"},"predicate":"SUPERSEDED_BY","object":{"id":70046142,"text":"70046142 - 1986 - Geohydrology of the Vamoosa-Ada aquifer east-central Oklahoma with a section on chemical quality of water","indexId":"70046142","publicationYear":"1986","noYear":false,"title":"Geohydrology of the Vamoosa-Ada aquifer east-central Oklahoma with a section on chemical quality of water"},"id":1}],"lastModifiedDate":"2023-09-20T00:19:18.616106","indexId":"70046142","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1986","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":244,"text":"Circular","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"87","title":"Geohydrology of the Vamoosa-Ada aquifer east-central Oklahoma with a section on chemical quality of water","docAbstract":"The Vamoosa-Ada aquifer, which underlies an area of about 2,320 mi2, consists principally of the Vamoosa Formation and the overlying Ada Group of Pennsylvanian age. Rocks comprising the aquifer were deposited in a nearshore environment ranging from marine on the west to nonmarine on the east. Because of changes in depositional environments with time and from place to place, the aquifer is a complex sequence of fine- to very fine-grained sandstone, siltstone, shale, and conglomerate, with interbedded very thin limestone. The aggregate thickness of water-bearing sandstones is greatest south of the Cimarron River, where it reaches a maximum of 550 ft in the vicinity of Seminole. North of the Cimarron River, the average aggregate thickness of the sandstones is about 100 ft, but locally it may be as much as 200 ft. Transmissivity values derived from seven aquifer tests made for this study range from 70 to 490 ft2 per day; values decrease from south to north with decreasing sandstone thickness. Hydraulic-conductivity values range from 2 to 4 ft per day. Storage coefficients for the confined part of the aquifer, as determined from four aquifer tests made during 1944, have an average value of 0.0002. The average storage coefficient for the unconfined part of the aquifer is estimated at 0.12, based on an analysis of geophysical logs and grain-size data. The specific capacity of wells tested is generally less than 1 gallon per minute per foot of drawdown. An approximate hydrologic budget for the aquifer for 1975 gives values, in acre-feet per year, of 93,000 for recharge, 233,000 for runoff, and 2,003,000 for evapotranspiration. The total of these values is almost equal to the average annual precipitation of 2,330,000 acre-ft per year. The estimated amount of water containing a maximum of 1,500 milligrams per liter of dissolved solids stored in the aquifer is estimated at 60 million acre-ft. Of this amount, an estimated 36 million acre-ft is available for use. The quality of water in the Vamoosa-Ada aquifer generally is suitable for municipal, domestic, and stock use. Of 55 water samples analyzed in the laboratory, about 75 percent were of the sodium bicarbonate or sodium calcium bicarbonate type; the remainder were of the sodium sulfate, calcium sulfate, sodium chloride, or indeterminate types. Laboratory and on-site chemical-quality data indicate that mineralization of both ground and surface waters is greater than normal in some areas. Water samples from 7 wells and 12 stream sites had concentrations of bromide exceeding 1 milligram per liter; the only known source of bromide in the area is brine associated with petroleum production.","language":"English","publisher":"Oklahoma Geological Survey","publisherLocation":"Reston, VA","collaboration":"Prepared by the United States Geological Survey in cooperation with the Oklahoma Geological Survey","usgsCitation":"D’Lugosz, J.J., McClaflin, R.G., and Marcher, M.V., 1986, Geohydrology of the Vamoosa-Ada aquifer east-central Oklahoma with a section on chemical quality of water: Circular 87, vi, 42 p.; Maps: 3 Sheets: 40 x 44 inches.","productDescription":"vi, 42 p.; Maps: 3 Sheets: 40 x 44 inches","numberOfPages":"48","costCenters":[{"id":634,"text":"Water Resources Program","active":false,"usgs":true}],"links":[{"id":272929,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.ou.edu/ogs/publications/circulars/circularssearch"},{"id":272933,"rank":2,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70046142.png"}],"country":"United States","state":"Oklahoma","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0,33.62 ], [ -103.0,37.0 ], [ -94.43,37.0 ], [ -94.43,33.62 ], [ -103.0,33.62 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51a5d1e9e4b0605bc571efbc","contributors":{"authors":[{"text":"D’Lugosz, Joseph J.","contributorId":71172,"corporation":false,"usgs":true,"family":"D’Lugosz","given":"Joseph","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":479029,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McClaflin, Roger G.","contributorId":50157,"corporation":false,"usgs":true,"family":"McClaflin","given":"Roger","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":479028,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Marcher, Melvin V.","contributorId":11590,"corporation":false,"usgs":true,"family":"Marcher","given":"Melvin","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":479027,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70043186,"text":"70043186 - 1986 - Bedrock aquifers of eastern San Juan County, Utah","interactions":[{"subject":{"id":12494,"text":"ofr85568 - 1985 - Bedrock aquifers of eastern San Juan County, Utah","indexId":"ofr85568","publicationYear":"1985","noYear":false,"title":"Bedrock aquifers of eastern San Juan County, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":70043186,"text":"70043186 - 1986 - Bedrock aquifers of eastern San Juan County, Utah","indexId":"70043186","publicationYear":"1986","noYear":false,"title":"Bedrock aquifers of eastern San Juan County, Utah"},"id":1}],"lastModifiedDate":"2016-12-13T09:44:27","indexId":"70043186","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1986","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":294,"text":"Technical Publication","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"86","title":"Bedrock aquifers of eastern San Juan County, Utah","docAbstract":"This study is one of a series of studies appraising the waterbearing properties of the Navajo Sandstone and associated formations in southern Utah. The stu<¥ area is al:x>dy area is about 4,600 square miles, extending from the Utah-Arizona State line northward to the San Juan-Grand County line and westward from the Utah-Colorado State line to the longitude of about 109°50'.
Some of the water-yielding formations are grouped into aquifer systems. The C aquifer is comprised of the DeChelly Sandstone Member of the Cutler Formation. The P aquifer is comprised of the Cedar Mesa Member of the Cutler Formation and the undifferentiated Cutler Formation. The N aquifer is comprised of the sedimentary section that includes the Wingate Sandstone, Kayenta Formation, Navajo Sandstone, Carmel Formation, and Entrada sandstone. The M aquifer is comprised of the Bluff Sandstone Member and other sandstone units of the Morrison Formation. The D aquifer is comprised of the Burro Canyon Formation and Dakota Sandstone. Discharge from the ground-water reservoir to the San Juan River between gaging stations at Four Corners and Mexican Hat is about 66 cubic feet per second.
The N aquifer is the main aquifer in the study area. Recharge by infiltration of precipitation is estimated to be 25,000 acre-feet per year. A major ground-water divide exists under the broad area east of Monticello. The thickness of the N aquifer, where the sedimentary section is fully preserved and saturated, generally is 750 to 1,250 feet. Hydraulic conductivity values obtained from aquifer tests range from 0.02 to 0.34 foot per day. The total volume of water in transient storage is about 11 million acre-feet. Well discharge somewhat exceeded 2,340 acre-feet during 1981. Discharge to the San Juan River from the N aquifer is estimated to be 6.9 cubic feet per second. Water quality ranges from a calcium bicarbonate to sodium chloride type water
","language":"English","publisher":"Utah Department of Natural Resources, Division of Water Rights","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared by the Unites States Geological Survey in cooperation with the Utah Department of Natural Resources and Energy Division of Water Rights","usgsCitation":"Avery, C., 1986, Bedrock aquifers of eastern San Juan County, Utah: Technical Publication 86, viii, 114 p.","productDescription":"viii, 114 p.","numberOfPages":"125","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":267104,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":332013,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://www.waterrights.utah.gov/cgi-bin/libview.exe?Modinfo=Viewpub&LIBNUM=20-6-200"},{"id":332014,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://waterrights.utah.gov/docSys/v920/w920/w92000ab.pdf"}],"country":"United States","state":"Utah","county":"San Juan County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.918212890625,\n 37.00255267215955\n ],\n [\n -109.918212890625,\n 38.74123075381228\n ],\n [\n -109.0447998046875,\n 38.74123075381228\n ],\n [\n -109.0447998046875,\n 37.00255267215955\n ],\n [\n -109.918212890625,\n 37.00255267215955\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5114dafce4b0ca7af0743b0c","contributors":{"authors":[{"text":"Avery, Charles","contributorId":70739,"corporation":false,"usgs":true,"family":"Avery","given":"Charles","affiliations":[],"preferred":false,"id":473124,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}