{"pageNumber":"61","pageRowStart":"1500","pageSize":"25","recordCount":1766,"records":[{"id":18274,"text":"ofr90379 - 1990 - A protocol for onsite screening of volatile organic compounds using a portable gas chromatograph","interactions":[],"lastModifiedDate":"2021-05-28T18:19:10.41313","indexId":"ofr90379","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1990","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":"90-379","title":"A protocol for onsite screening of volatile organic compounds using a portable gas chromatograph","docAbstract":"No abstract available.
","language":"English","publisher":"Dept. of the Interior, U.S. Geological Survey ; Denver, Colo.","doi":"10.3133/ofr90379","usgsCitation":"Brock, R., 1990, A protocol for onsite screening of volatile organic compounds using a portable gas chromatograph: U.S. Geological Survey Open-File Report 90-379, iv, 15 p., https://doi.org/10.3133/ofr90379.","productDescription":"iv, 15 p.","costCenters":[{"id":452,"text":"National Water Quality Laboratory","active":true,"usgs":true}],"links":[{"id":151183,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1990/0379/report-thumb.jpg"},{"id":47627,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1990/0379/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a87db","contributors":{"authors":[{"text":"Brock, R.D.","contributorId":12874,"corporation":false,"usgs":true,"family":"Brock","given":"R.D.","email":"","affiliations":[],"preferred":false,"id":178831,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":29026,"text":"wri904092 - 1990 - Hydrogeology and preliminary assessment of the potential for contamination of the Memphis aquifer in the Memphis area, Tennessee","interactions":[],"lastModifiedDate":"2012-02-02T00:08:49","indexId":"wri904092","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1990","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":"90-4092","title":"Hydrogeology and preliminary assessment of the potential for contamination of the Memphis aquifer in the Memphis area, Tennessee","docAbstract":"Detailed maps of the thickness of the\r\nJackson-upper Claibome confining unit and the\r\naltitude of the water table in the alluvium andfluvial\r\ndeposits provide much new information concerning\r\nareas where downward leakage is or may be\r\noccurringfrom the water-table aquifers to theMemphrj\r\naqutyer in the Memphis area. A detailed map\r\nof the altitude of the potentiometric surface of the\r\nMemphis aquifer and the locations of 44sites where\r\ncontaminants have been detected in the water-table\r\naquifers indicate that many of these sites are located\r\nin areas where the direction of ground-water flow in\r\nthe Memphis aquifer is toward municipal well\r\nfields. Consequently, if contaminants enter the\r\nMemphis aquifer, a hydraulic potential exists for\r\ntheir transport to those wellfields.\r\nRecently (19&S-88), volatile organic compounds\r\nwere detected in water from five municipal\r\nwells screened in the Memphis aquifer - three in the\r\nAllen well field of the Memphis Light, Gas and\r\nWater Division at Memphis and two in the west well\r\nfield at Collierville. Concentrations of seven volatile\r\norganic compounds totaled about II microgramsperliterin\r\nasamplefrom one well in theAllen\r\nwellfield at Memphis, and the concentration of one\r\ncompound was 25 micrograms per liter in a sample\r\nj?om one well at Collierville. These are the first\r\nreported occurrences of synthetic organic compounds\r\nin the Memphis aquifer andprove that the\r\nprincipal aquifer in the Memphis area is vulnerable\r\nto contamination.","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBooks and Open-File Reports Section [distributor],","doi":"10.3133/wri904092","usgsCitation":"Parks, W.S., 1990, Hydrogeology and preliminary assessment of the potential for contamination of the Memphis aquifer in the Memphis area, Tennessee: U.S. Geological Survey Water-Resources Investigations Report 90-4092, iv, 39 p. :ill., maps (some col.) ;28 cm., https://doi.org/10.3133/wri904092.","productDescription":"iv, 39 p. :ill., maps (some col.) ;28 cm.","costCenters":[],"links":[{"id":2293,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wri904092/","linkFileType":{"id":5,"text":"html"}},{"id":159409,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":57887,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4092/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57888,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4092/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57889,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4092/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57890,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4092/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b17e4b07f02db6a642b","contributors":{"authors":[{"text":"Parks, W. S.","contributorId":99555,"corporation":false,"usgs":true,"family":"Parks","given":"W.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":200814,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":29339,"text":"wri904028 - 1990 - Geohydrology and water quality of Kalamazoo County, Michigan, 1986-88","interactions":[],"lastModifiedDate":"2017-01-25T13:35:26","indexId":"wri904028","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1990","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":"90-4028","title":"Geohydrology and water quality of Kalamazoo County, Michigan, 1986-88","docAbstract":"Thick, glacial sand and gravel deposits provide most ground-water supplies in Kalamazoo County. These deposits range in thickness from 50 to about 600 feet in areas that overlie buried bedrock valleys. Most domestic wells completed at depths of less than 75 feet in the sands and gravels yield adequate water supplies. Most industry, public supply, and irrigation wells completed at depths of 100 to 200 feet yield 1,000 gallons per minute or more. The outwash plains include the most productive of the glacial aquifers in the county. The Coldwater Shale of Mississippian age, which underlies the glacial deposits in most of the county, usually yields only small amounts of largely mineralized water.
Ground-water levels in Kalamazoo County reflect short- and long-term changes in precipitation and local pumpage. Ground-water levels increase in the spring and decline in the fall.
Ground-water recharge rates, for different geologic settings, were estimated from ground-water runoff to the streams. Recharge rates ranged from 10.86 to 5.87 inches per year. A countywide-average ground-water recharge rate is estimated to be 9.32 inches per year.
Chemical quality of precipitation and dry fallout at two locations in Kalamazoo County were similar to that of other areas in the State. Total deposition of dissolved sulfate is 30.7 pounds per acre per year, of total nitrogen is 13.2 pounds per acre per year, and of total phosphorus is 0.3 pounds per acre per year. Rainfall and snow data indicated that the pH of precipitation is inversely proportional to its specific conductance.
Water of streams and rivers of Kalamazoo County is predominately of the calcium bicarbonate type, although dissolved sulfate concentrations are slightly larger in streams in the southeastern and northwestern parts of the county. The water in most streams is hard to very hard. Concentrations of dissolved chloride in streams draining urban-industrial areas are slightly larger than at other locations. Concentrations of total nitrogen and total phosphorus in streams are directly proportional to streamflow. Except for elevated concentrations of iron, none of the trace elements in streams exceeded maximum contaminant levels for drinking water established by the U.S. Environmental Protection Agency. Pesticides were detected in some streams.
Ground water in the surficial aquifers is of the calcium bicarbonate type, although sodium, sulfate, and chloride ions predominate at some locations. Specific conductance and hardness and concentrations of total dissolved-solids slightly exceed statewide averages. Concentrations of dissolved sodium and dissolved chloride in 6 wells were greater than most natural ground waters in the State, indicating possible contamination from road salts. Water samples from 6 of the 46 wells sampled contained concentrations of total nitrate as nitrogen greater than 10.0 milligrams per liter. Elevated concentrations of total nitrate as nitrogen in water from wells in rural-agricultural areas probably are related to fertilizer applications. Results of partial chemical analyses by the Michigan Department of Public Health indicates specific conductance, and concentrations of hardness, dissolved fluoride, and total iron are fairly uniform throughout the county. Concentrations of dissolved sodium, dissolved chloride, and total nitrate as nitrogen differed among townships. Pesticides were detected in water from only one well. Water from five wells contained volatile organics.
A map of susceptibility of ground water to contamination in Kalamazoo County was developed using a system created by the U.S. Environmental Protection Agency. Seven geohydrologic factors that affect and control ground-water movement are mapped and composited onto a countywide map. All seven factors have some effect on countywide susceptibility, but the most important factors are depth to water and composition of the materials above the aquifer.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Lansing, MI","doi":"10.3133/wri904028","collaboration":"Prepared in cooperation with Michigan Department of Natural Resources, Geological Survey Division, and Kalamazoo County","usgsCitation":"Rheaume, S.J., 1990, Geohydrology and water quality of Kalamazoo County, Michigan, 1986-88: U.S. Geological Survey Water-Resources Investigations Report 90-4028, Document: x, 102 p.; 3 Plates: 39.20 x 33.65 inches or smaller, https://doi.org/10.3133/wri904028.","productDescription":"Document: x, 102 p.; 3 Plates: 39.20 x 33.65 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":58182,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4028/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":58183,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4028/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":58184,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1990/4028/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":58185,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1990/4028/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":121811,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1990/4028/report-thumb.jpg"}],"country":"United States","state":"Michigan","county":"Kalamazoo County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-85.5421,42.4195],[-85.5328,42.4194],[-85.4172,42.4199],[-85.3091,42.4185],[-85.2979,42.4188],[-85.2969,42.3361],[-85.297,42.3298],[-85.2967,42.2721],[-85.296,42.2448],[-85.295,42.159],[-85.2928,42.0717],[-85.4102,42.0714],[-85.5301,42.0714],[-85.6427,42.0704],[-85.7638,42.0698],[-85.7654,42.157],[-85.7663,42.4196],[-85.5421,42.4195]]]},\"properties\":{\"name\":\"Kalamazoo\",\"state\":\"MI\"}}]}\n","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8bbd","contributors":{"authors":[{"text":"Rheaume, S. J.","contributorId":70804,"corporation":false,"usgs":true,"family":"Rheaume","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":201372,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70206239,"text":"70206239 - 1990 - Preliminary delineation of contaminated water-bearing fractures intersected by open-hole bedrock wells","interactions":[],"lastModifiedDate":"2019-10-25T12:49:45","indexId":"70206239","displayToPublicDate":"1990-11-30T12:40:12","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1866,"text":"Groundwater Monitoring & Remediation","active":true,"publicationSubtype":{"id":10}},"title":"Preliminary delineation of contaminated water-bearing fractures intersected by open-hole bedrock wells","docAbstract":"Contaminated water‐bearing fractures intersected by open‐hole bedrock wells were preliminarily delineated through a combination of geophysical logging, vertical‐flow measurements, and downhole water sampling as part of remedial site investigations in southeastern New York. The wells investigated range from 100 to 450 feet in depth, have only shallow surface casing, and intersect multiple water‐bearing zones. The distribution of water‐bearing zones that intersect the wells was determined from single‐point resistance, caliper, fluid‐resistivity, temperature, and acoustic‐televiewer logs. Measurable flow in the wells was downward from upper producing zones to lower receiving zones that are poorly connected in the aquifer and that differ in hydraulic head as a result of nearby pumping. A down hole sampler was used to collect discrete and composite water samples for analysis of volatile organic compounds from producing zones that are self‐purging as a result of flow in the wells.
The results obtained at two of the study sites are presented—the Spring Valley wellfield and the Mahopac business district. At the Spring Valley wellfield, a supply well completed in Mesozoic sandstone and conglomerate intersects water‐bearing zones at depths of 204 to 245 feet that produced contaminated water that was received by a zone at 278 feet. In the same well, a deeper zone at 345 feet produced uncontaminated water that was received by a zone at 403 feet. Correlation of information from the well, geophysical logs and drill cores from nearby monitoring wells, and bedrock outcrops indicates that most of the water‐bearing zones are bedding‐plane separations that probably provide pathways for contaminant transport in the bedrock aquifer for significant distances.
In the Mahopac business district, a deep test well completed in Precambrian gneiss intersected shallow waterbearing zones at 50 to 79 feet that produced contaminated water that was received by deep zones at 260 and 328 feet. The water‐bearing zones consist of single or closely spaced multiple fractures with dips of 5 to 50 degrees. By analogy with the results from this test well, deep open‐hole wells in the area may serve as “short circuits” in the ground water flow system and allow direct transport of contaminants to deeper zones in the fractured‐bedrock aquifer.
The methods presented can be used to investigate ground water flow and contamination in fractured‐bedrock aquifers in advance of more focused monitoring programs. The methods can be applied in existing open‐hole wells before test drilling and monitoring well installation to provide for efficient program design. The methods also can be used during the installation of monitoring wells to help determine completion depths and open intervals and to ensure that the wells are not serving as conduits for the flow of contaminated water.
","language":"English","publisher":"National Groundwater Association","doi":"10.1111/j.1745-6592.1990.tb00028.x","usgsCitation":"Williams, J., and Conger, R.W., 1990, Preliminary delineation of contaminated water-bearing fractures intersected by open-hole bedrock wells: Groundwater Monitoring & Remediation, v. 10, no. 4, p. 118-126, https://doi.org/10.1111/j.1745-6592.1990.tb00028.x.","productDescription":"9 p.","startPage":"118","endPage":"126","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true},{"id":493,"text":"Office of Ground Water","active":true,"usgs":true},{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":368615,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New York","city":"Mahopec, Spring Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -74.0833854675293,\n 41.09435964868545\n ],\n [\n -74.02244567871092,\n 41.09435964868545\n ],\n [\n -74.02244567871092,\n 41.13988169508488\n ],\n [\n -74.0833854675293,\n 41.13988169508488\n ],\n [\n -74.0833854675293,\n 41.09435964868545\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.76581192016602,\n 41.36225128971916\n ],\n [\n -73.71585845947266,\n 41.36225128971916\n ],\n [\n -73.71585845947266,\n 41.40011918484133\n ],\n [\n -73.76581192016602,\n 41.40011918484133\n ],\n [\n -73.76581192016602,\n 41.36225128971916\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"10","issue":"4","noUsgsAuthors":false,"publicationDate":"2007-02-22","publicationStatus":"PW","contributors":{"authors":[{"text":"Williams, John 0000-0002-6054-6908 jhwillia@usgs.gov","orcid":"https://orcid.org/0000-0002-6054-6908","contributorId":1553,"corporation":false,"usgs":true,"family":"Williams","given":"John","email":"jhwillia@usgs.gov","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":true,"id":773907,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Conger, Randall W. rwconger@usgs.gov","contributorId":2086,"corporation":false,"usgs":true,"family":"Conger","given":"Randall","email":"rwconger@usgs.gov","middleInitial":"W.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":true,"id":773908,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70242100,"text":"70242100 - 1990 - Geochemistry of highly fractionated I- and S-type granites from the tin-tungsten province of western Tasmania","interactions":[],"lastModifiedDate":"2023-04-06T16:34:21.889197","indexId":"70242100","displayToPublicDate":"1990-01-01T11:26:00","publicationYear":"1990","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"seriesTitle":{"id":5614,"text":"Special Papers of the Geological Society of America","printIssn":"0072-1077","active":true,"publicationSubtype":{"id":24}},"title":"Geochemistry of highly fractionated I- and S-type granites from the tin-tungsten province of western Tasmania","docAbstract":"The Devonian batholiths of western Tasmania represent a diverse assemblage of highly fractionated intrusions (70 to 77 percent SiO2) that are the products of different source materials. The Housetop batholith exhibits compositional affinities to a fluorine-rich I-type magma. The Meredith batholith also has characteristics indicative of I-type source materials. The Heemskirk batholith is composite, and consists of a volatile (F, B, H2O)–rich S-type granite underlying an I-type granite. The Three Hummock Island, Interview River, Sandy Cape, and Conical Rocks plutons probably have an S-type source and are grouped together as the Sandy Cape Suite. Rapakivi texture is common in the Housetop, Meredith, and Heemkirk batholiths. Quartz-tourmaline nodules are found in the Conical Rocks pluton and the S-type portion of the Heemskirk batholith.
The Conical Rocks and Interview River plutons yield high initial Sr isotopic ratios of 0.74242 and 0.76009, respectively. The Housetop and Meredith batholiths yield the lowest initial Sr isotopic ratios of 0.71041 and 0.71445, respectively. The S-type portion of the Heemskirk batholith has an initial Sr isotopic ratio of 0.76387. The 40Ar/39Ar release spectrum and Rb/Sr mineral isochron analyses corroborate previously reported Devonian to Carboniferous age estimates for these batholiths. A relatively low-temperature thermal event (<200°C) caused argon loss from the K-feldspars at about 105 Ma. This heating event is probably related to the continental breakup of Australia from Antarctica.
Major-element compositions of the western Tasmanian granites are very similar. The highly fractionated Sandy Cape Suite leucogranites exhibit high Ga/Al ratios typical of A-type granites, but not their extreme Zr, Y, or Ce enrichments. A distinctive feature of the Sandy Cape Suite is the increase in P2O5 concentration with fractionation. The increase in P2O5 with fractionation is apparently due to extremely low Ca activity, which precludes the formation of apatite, thus allowing P2O5 to behave incompatibly in the melt. All of the granitoids have LREE–enriched chondrite-normalized rare earth element patterns. REE fractionation within the individual granitoids can be summarized by two trends: those with LREE >> HREE depletion (Housetop, Meredith, and Heemskirk batholiths), and those with LREE = HREE depletion (Sandy Cape Suite). The first trend is caused by the initial undersaturation of accessory mineral assemblage that resulted from high concentrations of volatiles and/or alkali complexes. The second trend is caused by early saturation of accessory phases and/or refractory accessory phases.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Ore-bearing granite systems; petrogenesis and mineralizing processes","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Geological Society of America","doi":"10.1130/SPE246-p161","usgsCitation":"Sawka, W.N., Heizler, M., Kistler, R.W., and Chappell, B.W., 1990, Geochemistry of highly fractionated I- and S-type granites from the tin-tungsten province of western Tasmania, chap. of Ore-bearing granite systems; petrogenesis and mineralizing processes: Special Papers of the Geological Society of America, v. 246, p. 161-180, https://doi.org/10.1130/SPE246-p161.","productDescription":"20 p.","startPage":"161","endPage":"180","costCenters":[],"links":[{"id":415345,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Australia","state":"Tasmania","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n 145.39023502074014,\n -42.924046670787085\n ],\n [\n 146.4009772082385,\n -42.907954935315956\n ],\n [\n 146.35703189573798,\n -41.103979907033214\n ],\n [\n 145.35727603636406,\n -40.80528184932509\n ],\n [\n 145.34628970823962,\n -40.705415624950284\n ],\n [\n 145.11557681761525,\n -40.68875667127033\n ],\n [\n 144.9617682238648,\n -40.312829649092045\n ],\n [\n 144.62119205199053,\n -40.47181134072364\n ],\n [\n 144.55527408323843,\n -40.93820338749863\n ],\n [\n 144.67612369261553,\n -41.450751481905776\n ],\n [\n 144.87387759886377,\n -41.771102800345915\n ],\n [\n 145.14853580198866,\n -42.049084666908406\n ],\n [\n 145.11557681761525,\n -42.18762149297865\n ],\n [\n 145.39023502074014,\n -42.924046670787085\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"246","noUsgsAuthors":false,"publicationDate":"1990-01-01","publicationStatus":"PW","contributors":{"editors":[{"text":"Stein, Holly J.","contributorId":46959,"corporation":false,"usgs":true,"family":"Stein","given":"Holly J.","affiliations":[],"preferred":false,"id":868901,"contributorType":{"id":2,"text":"Editors"},"rank":1},{"text":"Hannah, Judith L.","contributorId":156397,"corporation":false,"usgs":false,"family":"Hannah","given":"Judith","email":"","middleInitial":"L.","affiliations":[{"id":20340,"text":"Colorado State University and CEED Centre of Excellence, University of Oslo","active":true,"usgs":false}],"preferred":false,"id":868902,"contributorType":{"id":2,"text":"Editors"},"rank":2}],"authors":[{"text":"Sawka, Wayne N.","contributorId":40592,"corporation":false,"usgs":true,"family":"Sawka","given":"Wayne","email":"","middleInitial":"N.","affiliations":[],"preferred":false,"id":868897,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Heizler, M.T.","contributorId":94799,"corporation":false,"usgs":true,"family":"Heizler","given":"M.T.","email":"","affiliations":[],"preferred":false,"id":868898,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kistler, R. W.","contributorId":36112,"corporation":false,"usgs":true,"family":"Kistler","given":"R.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":868899,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Chappell, B. W.","contributorId":72444,"corporation":false,"usgs":true,"family":"Chappell","given":"B.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":868900,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70016199,"text":"70016199 - 1990 - Prediction of stream volatilization coefficients","interactions":[],"lastModifiedDate":"2019-10-17T15:54:36","indexId":"70016199","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2255,"text":"Journal of Environmental Engineering","active":true,"publicationSubtype":{"id":10}},"title":"Prediction of stream volatilization coefficients","docAbstract":"Equations are developed for predicting the liquid-film and gas-film reference-substance parameters for quantifying volatilization of organic solutes from streams. Molecular weight and molecular-diffusion coefficients of the solute are used as correlating parameters. Equations for predicting molecular-diffusion coefficients of organic solutes in water and air are developed, with molecular weight and molal volume as parameters. Mean absolute errors of prediction for diffusion coefficients in water are 9.97% for the molecular-weight equation, 6.45% for the molal-volume equation. The mean absolute error for the diffusion coefficient in air is 5.79% for the molal-volume equation. Molecular weight is not a satisfactory correlating parameter for diffusion in air because two equations are necessary to describe the values in the data set. The best predictive equation for the liquid-film reference-substance parameter has a mean absolute error of 5.74%, with molal volume as the correlating parameter. The best equation for the gas-film parameter has a mean absolute error of 7.80%, with molecular weight as the correlating parameter.","language":"English","publisher":"ASCE","doi":"10.1061/(ASCE)0733-9372(1990)116:3(615)","issn":"07339372","usgsCitation":"Rathbun, R.E., 1990, Prediction of stream volatilization coefficients: Journal of Environmental Engineering, v. 116, no. 3, p. 615-631, https://doi.org/10.1061/(ASCE)0733-9372(1990)116:3(615).","productDescription":"17 p.","startPage":"615","endPage":"631","numberOfPages":"17","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":222999,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"116","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a81f3e4b0c8380cd7b80a","contributors":{"authors":[{"text":"Rathbun, Ronald E.","contributorId":59952,"corporation":false,"usgs":true,"family":"Rathbun","given":"Ronald","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":372815,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70171429,"text":"70171429 - 1990 - Organic contamination of ground water at Gas Works Park, Seattle, Washington","interactions":[],"lastModifiedDate":"2019-10-04T13:31:46","indexId":"70171429","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1866,"text":"Groundwater Monitoring & Remediation","active":true,"publicationSubtype":{"id":10}},"title":"Organic contamination of ground water at Gas Works Park, Seattle, Washington","docAbstract":"\n
Gas Works Park, in Seattle, Washington, is located on the site of a coal and oil gasification plant that ceased operation in 1956. During operation, many types of wastes, including coal, tar, and oil, accumulated on-site. The park soil is currently (1986) contaminated with compounds such as polynuclear aromatic hydrocarbons, volatile organic compounds, trace metals, and cyanide. Analyses of water samples from a network of observation wells in the park indicate that these compounds are also present in the ground water.
\n
\n
Polynuclear aromatic hydrocarbons and volatile organic compounds were identified in ground water samples in concentrations as large as 200 mg/L. Concentrations of organic compounds were largest where ground water was in contact with a non-aqueous phase liquid in the soil. Where no non-aqueous phase liquid was present, concentrations were much smaller, even if the ground water was in contact with contaminated soils. This condition is attributed to weathering processes in which soluble, low-molecular-weight organic compounds are preferentially dissolved from the non-aqueous phase liquid into the ground water. Where no non-aqueous phase liquid is present, only stained soils containing relatively insoluble, high-molecular-weight compounds remain. Concentrations of organic contaminants in the soils may still remain large.
\n
A bimodal volcanic suite with K![\"single](\"https://sdfestaticassets-us-east-1.sciencedirectassets.com/shared-assets/55/entities/sbnd.gif\")
Ar ages of 0.05–1.40 Ma was collected from the Sumisu Rift using alvin. These rocks are contemporaneous with island arc tholeiite lavas of the Izu-Ogasawara arc 20 km to the east, and provide a present day example of volcanism associated with arc rifting and back-arc basin initiation. Major element geochemistry of the basalts is most similar to that of basalts found in other, more mature back-arc basins, which indicates that back-arc basins need not begin their magmatic evolution with lavas bearing strong arc signatures.
Volatile concentrations distinguish Sumisu Rift basalts from island arc basalts and MORB. H2O contents, which are at least four times greater than in MORB, suppress plagioclase crystallization. This suppression results in a more mafic fractionating assemblage, which prevents Al2O3 depletion and delays the initiation of Fe2O3(tot) and TiO2 enrichment. However, unlike arc basalts,Fe3+/ΣFe ratios are only slightly higher than in MORB and are insufficient to cause magnetite saturation early enough to suppress Fe2O3(tot) and TiO2 enrichment. Thus, major element trends are more similar to those of MORB than arcs.
H2O, CO2 and S are undersaturated relative to pure phase solubility curves, indicating exsolution of an H2O-rich mixed gas phase. HighH2O/S, highδD, and low (MORB-like)δ34S ratios are considered primary and distinctive of the back-arc basin setting.
","language":"English","publisher":"Elsevier","doi":"10.1016/0012-821X(90)90184-Y","issn":"0012821X","usgsCitation":"Hochstaedter, A., Gill, J., Kusakabe, M., Newman, S., Pringle, M., Taylor, B., and Fryer, P., 1990, Volcanism in the Sumisu Rift, I. Major element, volatile, and stable isotope geochemistry: Earth and Planetary Science Letters, v. 100, no. 1-3, p. 179-194, https://doi.org/10.1016/0012-821X(90)90184-Y.","productDescription":"16 p.","startPage":"179","endPage":"194","numberOfPages":"16","costCenters":[],"links":[{"id":223037,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"100","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bc320e4b08c986b32af8a","contributors":{"authors":[{"text":"Hochstaedter, A.G.","contributorId":46693,"corporation":false,"usgs":true,"family":"Hochstaedter","given":"A.G.","email":"","affiliations":[],"preferred":false,"id":372295,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Gill, J.B.","contributorId":61171,"corporation":false,"usgs":true,"family":"Gill","given":"J.B.","email":"","affiliations":[],"preferred":false,"id":372296,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kusakabe, M.","contributorId":94437,"corporation":false,"usgs":true,"family":"Kusakabe","given":"M.","email":"","affiliations":[],"preferred":false,"id":372299,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Newman, S.","contributorId":7678,"corporation":false,"usgs":true,"family":"Newman","given":"S.","affiliations":[],"preferred":false,"id":372293,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Pringle, M.","contributorId":87694,"corporation":false,"usgs":true,"family":"Pringle","given":"M.","affiliations":[],"preferred":false,"id":372298,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Taylor, B.","contributorId":36683,"corporation":false,"usgs":true,"family":"Taylor","given":"B.","email":"","affiliations":[],"preferred":false,"id":372294,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Fryer, P.","contributorId":65995,"corporation":false,"usgs":true,"family":"Fryer","given":"P.","email":"","affiliations":[],"preferred":false,"id":372297,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}}
,{"id":70016277,"text":"70016277 - 1990 - High-density volatiles in the system C-O-H-N for the calibration of a laser Raman microprobe","interactions":[],"lastModifiedDate":"2024-04-11T16:34:08.504076","indexId":"70016277","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"High-density volatiles in the system C-O-H-N for the calibration of a laser Raman microprobe","docAbstract":"Three methods have been used to produce high-density volatiles in the system C-O-H-N for the calibration of a laser Raman microprobe (LRM): synthetic fluid-inclusion, sealed fused-quartz-tube, and high-pressure-cell methods. Because quantitative interpretation of a Raman spectrum of mixed-volatile fluid inclusions requires accurate knowledge of pressure- and composition-sensitive Raman scattering efficiencies or quantification factors for each species, calibrations of these parameters for mixtures of volatiles of known composition and pressure are necessary.
Two advantages of the synthetic fluid-inclusion method are that the inclusions can be used readily in complementary microthermometry (MT) studies and that they have sizes and optical properties like those in natural samples. Some disadvantages are that producing H2O-free volatile mixtures is difficult, the composition may vary from one inclusion to another, the exact composition and density of the inclusions are difficult to obtain, and the experimental procedures are complicated. The primary advantage of the method using sealed fused-quartz tubes is its simplicity. Some disadvantages are that exact compositions for complex volatile mixtures are difficult to predict, densities can be approximated only, and complementary MT studies on the tubes are difficult to conduct.
The advantages of the high-pressure-cell method are that specific, known compositions of volatile mixtures can be produced and that their pressures can be varied easily and are monitored during calibration. Some disadvantages are that complementary MT analysis is impossible, and the setup is bulky. Among the three methods for the calibration of an LRM, the high-pressure-cell method is the most reliable and convenient for control of composition and total pressure.
We have used the high-pressure cell to obtain preliminary data on
- 1.
(1) the ratio of the Raman quantification factors for CH4 and N2 in an equimolar CH4N2 mixture and
- 2.
(2) the spectral peak position of ν1 of CH4 in that mixture, as well as in pure CH4, at pressures up to 690 bars. These data were successfully applied to natural inclusions from the Duluth Complex in order to derive their compositions and total pressures.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(90)90350-T","issn":"00167037","usgsCitation":"Chou, I., Pasteris, J.D., and Seitz, J., 1990, High-density volatiles in the system C-O-H-N for the calibration of a laser Raman microprobe: Geochimica et Cosmochimica Acta, v. 54, no. 3, p. 535-543, https://doi.org/10.1016/0016-7037(90)90350-T.","productDescription":"9 p.","startPage":"535","endPage":"543","numberOfPages":"9","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":223561,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"54","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a30e6e4b0c8380cd5da4d","contributors":{"authors":[{"text":"Chou, I.-M. 0000-0001-5233-6479","orcid":"https://orcid.org/0000-0001-5233-6479","contributorId":44283,"corporation":false,"usgs":true,"family":"Chou","given":"I.-M.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":false,"id":373047,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pasteris, J. D.","contributorId":97640,"corporation":false,"usgs":false,"family":"Pasteris","given":"J.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":373048,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Seitz, J. C.","contributorId":102635,"corporation":false,"usgs":false,"family":"Seitz","given":"J. C.","affiliations":[],"preferred":false,"id":373049,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70016241,"text":"70016241 - 1990 - Comment on \"The surface of lo: A new model\" by Bruce Hapke","interactions":[],"lastModifiedDate":"2024-02-15T23:28:45.948699","indexId":"70016241","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1963,"text":"Icarus","active":true,"publicationSubtype":{"id":10}},"title":"Comment on \"The surface of lo: A new model\" by Bruce Hapke","docAbstract":"Hapke (1989, Icarus 79, 56–74) proposed that the surface of Io is dominantly basaltic with thin coatings of polysulfur oxide, S2O, ad SO,2. However, observations and models of the active volcanism indicate that volatiles such as sulfur and SO2 must be more abundant than envisioned by Hapke.
","language":"English","publisher":"Elsevier","doi":"10.1016/0019-1035(90)90171-5","issn":"00191035","usgsCitation":"McEwen, A.S., and Lunine, J., 1990, Comment on \"The surface of lo: A new model\" by Bruce Hapke: Icarus, v. 84, no. 1, p. 268-274, https://doi.org/10.1016/0019-1035(90)90171-5.","productDescription":"7 p.","startPage":"268","endPage":"274","numberOfPages":"7","costCenters":[],"links":[{"id":222950,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"84","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f7e8e4b0c8380cd4cd8e","contributors":{"authors":[{"text":"McEwen, A. S.","contributorId":11317,"corporation":false,"usgs":true,"family":"McEwen","given":"A.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":372942,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lunine, J. I.","contributorId":51899,"corporation":false,"usgs":false,"family":"Lunine","given":"J. I.","affiliations":[],"preferred":false,"id":372943,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70016194,"text":"70016194 - 1990 - The Taylor Creek Rhyolite of New Mexico: a rapidly emplaced field of lava domes and flows","interactions":[],"lastModifiedDate":"2012-03-12T17:18:40","indexId":"70016194","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1109,"text":"Bulletin of Volcanology","active":true,"publicationSubtype":{"id":10}},"title":"The Taylor Creek Rhyolite of New Mexico: a rapidly emplaced field of lava domes and flows","docAbstract":"The Tertiary Taylor Creek Rhyolite of southwest New Mexico comprises at least 20 lava domes and flows. Each of the lavas was erupted from its own vent, and the vents are distributed throughout a 20 km by 50 km area. The volume of the rhyolite and genetically associated pyroclastic deposits is at least 100 km3 (denserock equivalent). The rhyolite contains 15%-35% quartz, sanidine, plagioclase, ??biotite, ??hornblende phenocrysts. Quartz and sanidine account for about 98% of the phenocrysts and are present in roughly equal amounts. With rare exceptions, the groundmass consists of intergrowths of fine-grained silica and alkali feldspar. Whole-rock major-element composition varies little, and the rhyolite is metaluminous to weakly peraluminous; mean SiO2 content is about 77.5??0.3%. Similarly, major-element compositions of the two feldsparphenocryst species also are nearly constant. However, whole-rock concentrations of some trace-elements vary as much as several hundred percent. Initial radiometric age determinations, all K-Ar and fission track, suggest that the rhyolite lava field grew during a period of at least 2 m.y. Subsequent 40Ar/39Ar ages indicate that the period of growth was no more than 100 000 years. The time-space-composition relations thus suggest that the Taylor Creek Rhyolite was erupted from a single magma reservoir whose average width was at least 30 km, comparable in size to several penecontemporaneous nearby calderas. However, this rhyolite apparently is not related to a caldera structure. Possibly, the Taylor Creek Phyolite magma body never became sufficiently volatile rich to produce a large-volume pyroclastic eruption and associated caldera collapse, but instead leaked repeatedly to feed many relatively small domes and flows. The new 40Ar/39Ar ages do not resolve preexisting unknown relative-age relations among the domes and flows of the lava field. Nonetheless, the indicated geologically brief period during which Taylor Creek Rhyolite magma was erupted imposes useful constraints for future evaluation of possible models for petrogenesis and the origin of trace-element characteristics of the system. ?? 1990 Springer-Verlag.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Bulletin of Volcanology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Springer-Verlag","doi":"10.1007/BF00268927","issn":"02588900","usgsCitation":"Duffield, W.A., and Dalrymple, G.B., 1990, The Taylor Creek Rhyolite of New Mexico: a rapidly emplaced field of lava domes and flows: Bulletin of Volcanology, v. 52, no. 6, p. 475-487, https://doi.org/10.1007/BF00268927.","startPage":"475","endPage":"487","numberOfPages":"13","costCenters":[],"links":[{"id":222945,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":205317,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00268927"}],"volume":"52","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505ba918e4b08c986b322055","contributors":{"authors":[{"text":"Duffield, W. A.","contributorId":71935,"corporation":false,"usgs":true,"family":"Duffield","given":"W.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":372803,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dalrymple, G. B.","contributorId":10407,"corporation":false,"usgs":true,"family":"Dalrymple","given":"G.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":372802,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70016006,"text":"70016006 - 1990 - Production of sulfur gases and carbon dioxide by synthetic weathering of crushed drill cores from the Santa Cruz porphyry copper deposit near Casa Grande, Pinal County, Arizona","interactions":[],"lastModifiedDate":"2024-04-17T23:34:38.683475","indexId":"70016006","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2302,"text":"Journal of Geochemical Exploration","active":true,"publicationSubtype":{"id":10}},"title":"Production of sulfur gases and carbon dioxide by synthetic weathering of crushed drill cores from the Santa Cruz porphyry copper deposit near Casa Grande, Pinal County, Arizona","docAbstract":"Samples of ground drill cores from the southern part of the Santa Cruz porphyry copper deposit, Casa Grande, Arizona, were oxidized in simulated weathering experiments. The samples were also separated into various mineral fractions and analyzed for contents of metals and sulfide minerals. The principal sulfide mineral present was pyrite.
Gases produced in the weathering experiments were measured by gas chromatography. Carbon dioxide, oxygen, carbonyl sulfide, sulfur dioxide and carbon disulfide were found in the gases; no hydrogen sulfide, organic sulfides, or mercaptans were detected. Oxygen concentration was very important for production of the volatiles measured; in general, oxygen concentration was more important to gas production than were metallic element content, sulfide mineral content, or mineral fraction (oxide or sulfide) of the sample. The various volatile species also appeared to be interactive; some of the volatiles measured may have been formed through gas reactions.
","language":"English","publisher":"Elsevier","doi":"10.1016/0375-6742(90)90092-O","issn":"03756742","usgsCitation":"Hinkle, M.E., Ryder, J.L., Sutley, S.J., and Botinelly, T., 1990, Production of sulfur gases and carbon dioxide by synthetic weathering of crushed drill cores from the Santa Cruz porphyry copper deposit near Casa Grande, Pinal County, Arizona: Journal of Geochemical Exploration, v. 38, no. 1-2, p. 43-67, https://doi.org/10.1016/0375-6742(90)90092-O.","productDescription":"25 p.","startPage":"43","endPage":"67","numberOfPages":"25","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":223243,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"38","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a8de6e4b0c8380cd7eece","contributors":{"authors":[{"text":"Hinkle, M. E.","contributorId":11612,"corporation":false,"usgs":true,"family":"Hinkle","given":"M.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":372323,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ryder, J. L.","contributorId":30997,"corporation":false,"usgs":true,"family":"Ryder","given":"J.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":372325,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sutley, S. J.","contributorId":91484,"corporation":false,"usgs":true,"family":"Sutley","given":"S.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":372326,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Botinelly, T.","contributorId":20408,"corporation":false,"usgs":true,"family":"Botinelly","given":"T.","affiliations":[],"preferred":false,"id":372324,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70016139,"text":"70016139 - 1990 - Determination of trace concentrations of volatile organic compounds in ground water using closed-loop stripping, Edwards aquifer, Texas","interactions":[],"lastModifiedDate":"2023-10-30T12:24:36.620673","indexId":"70016139","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1103,"text":"Bulletin of Environmental Contamination and Toxicology","active":true,"publicationSubtype":{"id":10}},"title":"Determination of trace concentrations of volatile organic compounds in ground water using closed-loop stripping, Edwards aquifer, Texas","docAbstract":"No abstract available.
","language":"English","publisher":"Springer","doi":"10.1007/BF01700622","issn":"00074861","usgsCitation":"Buszka, P., Zaugg, S., and Werner, M., 1990, Determination of trace concentrations of volatile organic compounds in ground water using closed-loop stripping, Edwards aquifer, Texas: Bulletin of Environmental Contamination and Toxicology, v. 45, no. 4, p. 507-515, https://doi.org/10.1007/BF01700622.","productDescription":"9 p.","startPage":"507","endPage":"515","numberOfPages":"9","costCenters":[{"id":452,"text":"National Water Quality Laboratory","active":true,"usgs":true}],"links":[{"id":222781,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -98.88401760620185,\n 29.112556868650884\n ],\n [\n -97.41184963745192,\n 29.112556868650884\n ],\n [\n -97.41184963745192,\n 30.63671198227594\n ],\n [\n -98.88401760620185,\n 30.63671198227594\n ],\n [\n -98.88401760620185,\n 29.112556868650884\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"45","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ffe1e4b0c8380cd4f450","contributors":{"authors":[{"text":"Buszka, P.M.","contributorId":49001,"corporation":false,"usgs":true,"family":"Buszka","given":"P.M.","affiliations":[],"preferred":false,"id":372644,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zaugg, S.D.","contributorId":82811,"corporation":false,"usgs":true,"family":"Zaugg","given":"S.D.","email":"","affiliations":[],"preferred":false,"id":372645,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Werner, M.G.","contributorId":47400,"corporation":false,"usgs":true,"family":"Werner","given":"M.G.","email":"","affiliations":[],"preferred":false,"id":372643,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70016322,"text":"70016322 - 1990 - Evaluation of gases, condensates, and SO2 emissions from Augustine volcano, Alaska: the degassing of a Cl-rich volcanic system","interactions":[],"lastModifiedDate":"2012-03-12T17:18:54","indexId":"70016322","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1109,"text":"Bulletin of Volcanology","active":true,"publicationSubtype":{"id":10}},"title":"Evaluation of gases, condensates, and SO2 emissions from Augustine volcano, Alaska: the degassing of a Cl-rich volcanic system","docAbstract":"After the March-April 1986 explosive eruption a comprehensive gas study at Augustine was undertaken in the summers of 1986 and 1987. Airborne COSPEC measurements indicate that passive SO2 emission rates declined exponentially during this period from 380??45 metric tons/day (T/D) on 7/24/86 to 27??6 T/D on 8/24/87. These data are consistent with the hypothesis that the Augustine magma reservoir has become more degassed as volcanic activity decreased after the spring 1986 eruption. Gas samples collected in 1987 from an 870??C fumarole on the andesitic lava dome show various degrees of disequilibrium due to oxidation of reduced gas species and condensation (and loss) of H2O in the intake tube of the sampling apparatus. Thermochemical restoration of the data permits removal of these effects to infer an equilibrium composition of the gases. Although not conclusive, this restoration is consistent with the idea that the gases were in equilibrium at 870??C with an oxygen fugacity near the Ni-NiO buffer. These restored gas compositions show that, relative to other convergent plate volcanoes, the Augustine gases are very HCl rich (5.3-6.0 mol% HCl), S rich (7.1 mol% total S), and H2O poor (83.9-84.8 mol% H2O). Values of ??D and ??18O suggest that the H2O in the dome gases is a mixture of primary magmatic water (PMW) and local seawater. Part of the Cl in the Augustine volcanic gases probably comes from this shallow seawater source. Additional Cl may come from subducted oceanic crust because data by Johnston (1978) show that Cl-rich glass inclusions in olivine crystals contain hornblende, which is evidence for a deep source (>25km) for part of the Cl. Gas samples collected in 1986 from 390??-642??C fumaroles on a ramp surrounding the inner summit crater have been oxidized so severely that restoration to an equilibrium composition is not possible. H and O isotope data suggest that these gases are variable mixtures of seawater, FMW, and meteoric steam. These samples are much more H2O-rich (92%-97% H2O) than the dome gases, possibly due to a larger meteoric steam component. The 1986 samples also have higher Cl/S, S/C, and F/Cl ratios, which imply that the magmatic component in these gases is from the more degassed 1976 magma. Thus, the 1987 samples from the lava dome are better indicators than the 1986 samples of degassing within the Augustine magma reservoir, even though they were collected a year later and contain a significant seawater component. Future gas studies at Augustine should emphasize fumaroles on active lava domes. Condensates collected from the same lava-dome fumarole have enrichments ot 107-102 in Cl, Br, F, B, Cd, As, S, Bi, Pb, Sb, Mo, Zn, Cu, K, Li, Na, Si, and Ni. Lower-temperature (200??-650??C) fumaroles around the volcano are generally less enriched in highly volatile elements. However, these lower-termperature fumaroles have higher concentration of rock-forming elements, probably derived from the wall rock. ?? 1990 Springer-Verlag.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Bulletin of Volcanology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Springer-Verlag","doi":"10.1007/BF00302048","issn":"02588900","usgsCitation":"Symonds, R., Rose, W.I., Gerlach, T., Briggs, P., and Harmon, R., 1990, Evaluation of gases, condensates, and SO2 emissions from Augustine volcano, Alaska: the degassing of a Cl-rich volcanic system: Bulletin of Volcanology, v. 52, no. 5, p. 355-374, https://doi.org/10.1007/BF00302048.","startPage":"355","endPage":"374","numberOfPages":"20","costCenters":[],"links":[{"id":205386,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00302048"},{"id":223563,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"52","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0c77e4b0c8380cd52b72","contributors":{"authors":[{"text":"Symonds, R.B.","contributorId":31011,"corporation":false,"usgs":true,"family":"Symonds","given":"R.B.","email":"","affiliations":[],"preferred":false,"id":373178,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rose, William I. Jr.","contributorId":71556,"corporation":false,"usgs":true,"family":"Rose","given":"William","suffix":"Jr.","email":"","middleInitial":"I.","affiliations":[],"preferred":false,"id":373180,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Gerlach, T.M.","contributorId":38713,"corporation":false,"usgs":true,"family":"Gerlach","given":"T.M.","email":"","affiliations":[],"preferred":false,"id":373179,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Briggs, Paul H.","contributorId":107691,"corporation":false,"usgs":true,"family":"Briggs","given":"Paul H.","affiliations":[],"preferred":false,"id":373181,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Harmon, R.S.","contributorId":6585,"corporation":false,"usgs":true,"family":"Harmon","given":"R.S.","email":"","affiliations":[],"preferred":false,"id":373177,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}}
,{"id":70016303,"text":"70016303 - 1990 - Recent crustal subsidence at Yellowstone Caldera, Wyoming","interactions":[],"lastModifiedDate":"2012-03-12T17:18:41","indexId":"70016303","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1109,"text":"Bulletin of Volcanology","active":true,"publicationSubtype":{"id":10}},"title":"Recent crustal subsidence at Yellowstone Caldera, Wyoming","docAbstract":"Following a period of net uplift at an average rate of 15??1 mm/year from 1923 to 1984, the east-central floor of Yellowstone Caldera stopped rising during 1984-1985 and then subsided 25??7 mm during 1985-1986 and an additional 35??7 mm during 1986-1987. The average horizontal strain rates in the northeast part of the caldera for the period from 1984 to 1987 were: {Mathematical expression}1 = 0.10 ?? 0.09 ??strain/year oriented N33?? E??9?? and {Mathematical expression}2 = 0.20 ?? 0.09 ??strain/year oriented N57?? W??9?? (extension reckoned positive). A best-fit elastic model of the 1985-1987 vertical and horizontal displacements in the eastern part of the caldera suggests deflation of a horizontal tabular body located 10??5 km beneath Le Hardys Rapids, i.e., within a deep hydrothermal system or within an underlying body of partly molten rhyolite. Two end-member models each explain most aspects of historical unrest at Yellowstone, including the recent reversal from uplift to subsidence. Both involve crystallization of an amount of rhyolitic magma that is compatible with the thermal energy requirements of Yellowstone's vigorous hydrothermal system. In the first model, injection of basalt near the base of the rhyolitic system is the primary cause of uplift. Higher in the magmatic system, rhyolite crystallizes and releases all of its magmatic volatiles into the shallow hydrothermal system. Uplift stops and subsidence starts whenever the supply rate of basalt is less than the subsidence rate produced by crystallization of rhyolite and associated fluid loss. In the second model, uplift is caused primarily by pressurization of the deep hydrothermal system by magmatic gas and brine that are released during crystallization of rhyolite and them trapped at lithostatic pressure beneath an impermeable self-sealed zone. Subsidence occurs during episodic hydrofracturing and injection of pore fluid from the deep lithostatic-pressure zone into a shallow hydrostatic-pressure zone. Heat input from basaltic intrusions is required to maintain Yellowstone's silicic magmatic system and shallow hydrothermal system over time scales longer than about 105 years, but for the historical time period crystallization of rhyolite can account for most aspects of unrest at Yellowstone, including seismicity, uplift, subsidence, and hydrothermal activity. ?? 1990 Springer-Verlag.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Bulletin of Volcanology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Springer-Verlag","doi":"10.1007/BF00304098","issn":"02588900","usgsCitation":"Dzurisin, D., Savage, J., and Fournier, R., 1990, Recent crustal subsidence at Yellowstone Caldera, Wyoming: Bulletin of Volcanology, v. 52, no. 4, p. 247-270, https://doi.org/10.1007/BF00304098.","startPage":"247","endPage":"270","numberOfPages":"24","costCenters":[],"links":[{"id":205350,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00304098"},{"id":223207,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"52","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a95f3e4b0c8380cd81d1b","contributors":{"authors":[{"text":"Dzurisin, D.","contributorId":76067,"corporation":false,"usgs":true,"family":"Dzurisin","given":"D.","email":"","affiliations":[],"preferred":false,"id":373122,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Savage, J.C. 0000-0002-5114-7673","orcid":"https://orcid.org/0000-0002-5114-7673","contributorId":102876,"corporation":false,"usgs":true,"family":"Savage","given":"J.C.","affiliations":[],"preferred":false,"id":373123,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Fournier, R.O.","contributorId":73584,"corporation":false,"usgs":true,"family":"Fournier","given":"R.O.","email":"","affiliations":[],"preferred":false,"id":373121,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70159101,"text":"70159101 - 1989 - Water-quality data for the Potomac-Raritan-Magothy aquifer system in the northern coast plain of New Jersey, 1923-86","interactions":[],"lastModifiedDate":"2015-10-22T09:24:42","indexId":"70159101","displayToPublicDate":"2015-06-02T05:15:00","publicationYear":"1989","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesNumber":"19","title":"Water-quality data for the Potomac-Raritan-Magothy aquifer system in the northern coast plain of New Jersey, 1923-86","docAbstract":"Ground-water-quality data for the upper and middle aquifers of the Potomac-Raritan-Magothy aquifer system in Middlesex and Monmouth Counties are compiled for the period 1923-86. A total of 330 wells were sampled: 192 wells in the upper aquifer and 138 wells in the middle aquifer. Most of the complete water-quality analyses were collected after September 1984, as part of a regional ground-water assessment. Well-construction data for the sampled wells also are presented. Public-supply, domestic-supply, industrial, commercial, irrigation, and observation wells were sampled for the study. Field measurements made at the time of sample collection include water temperature, specific conductance , dissolved oxygen, pH, alkalinity, and bicarbonate concentration. Laboratory determinations include common ions, silica, dissolved solids, trace metals, volatile organic compounds, and pesticides. A quality-assurance program was followed to evaluate and assure the quality of the data.
\nThe report also contains a table of lithologic and hydrologic characteristics of the geologic units in the study area, a table of chloride concentrations and field measurements from 1923-86, and statistical summaries of selected water-quality data for the upper and middle aquifers. Many constituents were found in a wide range of concentrations.
\nWater from more than 25 percent of the wells sampled contained lead concentrations above the detection limit of 10 ug/L (micrograms per liter). Included in this number are some wells that had lead concentrations greater than the U.S. Environmental Protection Agency (USEPA) primary drinking-water regulation of 50 ug/L. Cadmium concentrations, although lower than lead concentrations, followed a similar pattern. Water from approximately 25 percent of the wells in the upper aquifer, contain cadmium concentrations equal to or greater than the detection limit of 1 ug/L.
\nDissolved iron concentrations ranged from 5 ug/L to 480,000 ug/L. Water from more than 50 percent of the wells sampled contained iron concentrations in excess of the USEPA secondary drinking-water recommended limit of 300 ug/L.
\nChloride concentrations greater than the USEPA secondary drinking-water recommended limit of 250 milligrams per liter were found in samples from wells located in the cities of Perth Amboy and South Amboy; in the boroughs of Keansburg, Sayreville, Keyport, and Union Beach; and in the townships of Old Bridge and Woodbridge.
\nOf 21 samples collected from wells screened in the upper aquifer and analyzed for 30 volatile organic compounds (VOCs), 5 samples contained at least 1 VOC at or above the detection limit. In the middle aquifer, 12 of the 21 samples collected and analyzed for VOCs contained at least 1 VOC greater than the detection limit.
\nConcentrations of pesticides generally were low. Of the 43 samples collected from wells screened in the upper aquifer and analyzed for pesticides, 4 samples contained concentrations of pesticides at or greater than the detection limit. In the middle aquifer, 6 of 38 samples collected and analyzed for 32 pesticides had at least 1 pesticide with a concentration greater than the detection limit.
\n
","language":"English","publisher":"U.S. Geological Survey","collaboration":"Prepared by the United States Geological Survey in cooperation with the New Jersey Department of Environmental Protection Division of Water Resources","usgsCitation":"Harriman, D.A., Pope, D.A., and Gordon, A.D., 1989, Water-quality data for the Potomac-Raritan-Magothy aquifer system in the northern coast plain of New Jersey, 1923-86, Report: iv, 94 p.; 2 Plates: 23.97 x 22.00 inches, 23.70 x 21.93 inches.","productDescription":"Report: iv, 94 p.; 2 Plates: 23.97 x 22.00 inches, 23.70 x 21.93 inches","numberOfPages":"100","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":309926,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70159101.jpg"},{"id":310333,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70159101/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}},{"id":310334,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70159101/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"}},{"id":310335,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70159101/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Jersey","county":"Middlesex County, Monmouth County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -74.6630859375,\n 40.1452892956766\n ],\n [\n -74.6630859375,\n 40.66813955408042\n ],\n [\n -73.94210815429688,\n 40.66813955408042\n ],\n [\n -73.94210815429688,\n 40.1452892956766\n ],\n [\n -74.6630859375,\n 40.1452892956766\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5620cedde4b06217fc478b48","contributors":{"authors":[{"text":"Harriman, Douglas A.","contributorId":70544,"corporation":false,"usgs":true,"family":"Harriman","given":"Douglas","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":577598,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pope, Daryll A. dpope@usgs.gov","contributorId":3796,"corporation":false,"usgs":true,"family":"Pope","given":"Daryll","email":"dpope@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":577599,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Gordon, Alison D. 0000-0002-9502-8633 agordon@usgs.gov","orcid":"https://orcid.org/0000-0002-9502-8633","contributorId":890,"corporation":false,"usgs":true,"family":"Gordon","given":"Alison","email":"agordon@usgs.gov","middleInitial":"D.","affiliations":[{"id":470,"text":"New Jersey Water Science Center","active":true,"usgs":true}],"preferred":true,"id":577600,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70157443,"text":"70157443 - 1989 - Hydrogeology of Wood County, Wisconsin","interactions":[],"lastModifiedDate":"2018-01-08T19:23:20","indexId":"70157443","displayToPublicDate":"2014-11-03T04:00:00","publicationYear":"1989","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":"60","title":"Hydrogeology of Wood County, Wisconsin","docAbstract":"The presence of low-permeability Precambrian rocks near land surface limits ground-water availability in the northern two-thirds of Wood County. Sand and gravel deposits provide large amounts of water (more than 500 gallons per minute) to some wells in the southeastern part of the county. Fine-grained unconsolidated deposits generally are less than 20 feet thick in the northern two-thirds of the county, but sand and gravel deposits 40- to 100-feet thick underlie the extreme southeastern part of the county. Horizontal hydraulic conductivity of the sand and gravel deposits ranges from about 155 to about 280 feet per day. The horizontal hydraulic conductivity of fine-grained unconsolidated deposits in the northern part of the county ranges from about 0.02 to 2 feet per day. Where unconsolidated deposits do not yield dependable water supplies, wells are finished in Precambrian rocks. Fractures occurring at shallow depths are the primary source of water for wells finished in Precambrian rocks. Because the number of fractures tends to decrease with depth, the horizontal hydraulic conductivity of these rocks generally decreases from about 11 feet per day in wells less than 50-feet deep to about 0.02 foot per day in wells greater than 160 feet deep.
\nEstimates of ground-water recharge to sand and gravel deposits in the southeastern part of the county range from about 7 to 12 inches per year. Recharge estimates for the central and northern parts of the county range from about 1 to 4 inches per year.
\nThe total dissolved-solids concentration in ground water in Wood County is relatively low. Concentrations in water samples from 124 wells ranged from 21 to 578 milligrams per liter, with a median concentration of about 190 milligrams per liter. Major dissolved constituents are calcium, magnesium, and bicarbonate; sodium, potassium, chloride, and sulfate are present in low concentrations. The most common water-quality problem in Wood County is elevated iron concentrations. Iron concentrations greater than 300 micrograms per liter were found in 54 of 124 samples, and 15 samples contained iron concentrations greater than 5,000 micrograms per liter.
\nNitrate as nitrogen concentrations exceeded Wisconsin's drinking-water standard (10 milligrams per liter) in water from just 4 of 124 wells. The pesticide aldicarb was detected in 7 of 36 samples, and various volatile organic compounds were detected in 24 of 102 ground-water samples collected by the Wisconsin Department of Natural Resources since 1980. Wells in which these chemicals were detected are near irrigated agricultural fields and in commercially developed areas where buried gasoline-storage tanks and chemical spills are more likely to occur.
\nA reconnaissance approach combining electromagnetic surveys and sampling for water-quality indicators was used to assess effects of leachate on ground water near seven landfills. Results of the electromagnetic surveys were used to site water-quality observation wells. Total dissolved-solids concentrations and concentrations of volatile organic compounds, chloride, sulfate, iron, chemical oxygen demand, and organic carbon are some of the chemical constituents analyzed in samples collected from these wells.
\nThe average rate of ground·water pumpage in Wood County in 1985 was 9.7 million gallons per day. Of this rate, about 6 million gallons per day is pumped from municipal-supply wells in seven communities.An additional 1.08 million gallons per day is pumped for agricultural irrigation.
","language":"English","publisher":"Wisconsin Geological & Natural History Survey","collaboration":"Prepared in cooperation with the University of Wisconsin-Extension, Geological and Natural History Survey, and Wood County","usgsCitation":"Batten, W.G., 1989, Hydrogeology of Wood County, Wisconsin: Wisconsin Geological & Natural History Survey Information Circular 60, vi, 27 p.","productDescription":"vi, 27 p.","numberOfPages":"33","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":308446,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":350382,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://wgnhs.uwex.edu/pubs/download_ic60/"}],"country":"United States","state":"Wisconsin","county":"Wood County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-89.8449,44.6849],[-89.8451,44.5983],[-89.8447,44.5116],[-89.7268,44.5114],[-89.7259,44.4239],[-89.7243,44.3372],[-89.7247,44.2479],[-89.8376,44.249],[-89.8982,44.2493],[-89.9557,44.2491],[-89.9908,44.249],[-90.073,44.2491],[-90.0807,44.2491],[-90.1675,44.2491],[-90.1924,44.249],[-90.1975,44.249],[-90.1994,44.249],[-90.3123,44.2497],[-90.3161,44.2497],[-90.3172,44.3377],[-90.3163,44.4247],[-90.3161,44.5127],[-90.3165,44.5989],[-90.3163,44.6852],[-90.1981,44.6854],[-90.0793,44.685],[-89.9644,44.685],[-89.8449,44.6849]]]},\"properties\":{\"name\":\"Wood\",\"state\":\"WI\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5603cd44e4b03bc34f544b10","contributors":{"authors":[{"text":"Batten, W. G.","contributorId":89504,"corporation":false,"usgs":true,"family":"Batten","given":"W.","email":"","middleInitial":"G.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":573196,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70015358,"text":"70015358 - 1989 - Gas transport in unsaturated porous media: The adequacy of Fick's law","interactions":[],"lastModifiedDate":"2025-07-21T16:39:06.758759","indexId":"70015358","displayToPublicDate":"2010-06-14T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3283,"text":"Reviews of Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"Gas transport in unsaturated porous media: The adequacy of Fick's law","docAbstract":"The increasing use of natural unsaturated zones as repositories for landfills and disposal sites for hazardous wastes (chemical and radioactive) requires a greater understanding of transport processes in the unsaturated zone. For volatile constituents an important potential transport mechanism is gaseous diffusion. Diffusion, however, cannot be treated as an independent isolated transport mechanism. A complete understanding of multicomponent gas transport in porous media (unsaturated zones) requires a knowledge of Knudsen transport, the molecular and nonequimolar components of diffusive flux, and viscous (pressure driven) flux. The constitutive equations relating these flux components are available from the “dusty gas” model of Mason et al. (1967). This review presents a brief discussion of the underlying principles and interrelationships among each of the above flux mechanisms. Some aspects of these transport mechanisms are, to our knowledge, generally unrecognized in the Earth science literature. The principles underlying the transport mechanisms are illustrated with binary systems; the constitutive equations are then cast in forms thought to be most useful for the study of natural unsaturated zones. The viscous and diffusive fluxes are coupled in the constitutive equations through the Knudsen diffusivities; a knowledge of Knudsen diffusivities is necessary to calculate the viscous component of flux and pressure gradients. The Knudsen diffusivities can be calculated from measurements of the Klinkenberg effect. Two examples are presented showing that in natural systems, very small pressure gradients (1 Pa/m or less) can produce viscous fluxes greater than or equal to diffusive fluxes and that, conversely, pressure gradients of this magnitude can be generated by diffusive processes. The example calculations show that major concentration gradients can be developed for stagnant (zero flux, nonreactive) gases. A method is presented for approximating the viscous and diffusive flux components of gases in a multicomponent system from a knowledge of the concentration profiles of stagnant gases. In subsoil environments, argon and nitrogen are considered to be stagnant gases. Fick's laws are essentially, by definition, inadequate to deal with stagnant gases. In the examples presented, the error associated with estimating the total fluxes of nonstagnant gases by Fick's law, relative to stationary coordinates, ranges from a few percent to orders of magnitude.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/RG027i001p00061","issn":"87551209","usgsCitation":"Thorstenson, D., and Pollock, D., 1989, Gas transport in unsaturated porous media: The adequacy of Fick's law: Reviews of Geophysics, v. 27, no. 1, p. 61-78, https://doi.org/10.1029/RG027i001p00061.","productDescription":"18 p.","startPage":"61","endPage":"78","costCenters":[],"links":[{"id":224364,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"27","issue":"1","noUsgsAuthors":false,"publicationDate":"2010-06-14","publicationStatus":"PW","scienceBaseUri":"505a14d8e4b0c8380cd54bc8","contributors":{"authors":[{"text":"Thorstenson, D.C.","contributorId":47377,"corporation":false,"usgs":true,"family":"Thorstenson","given":"D.C.","email":"","affiliations":[],"preferred":false,"id":370734,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pollock, D.W.","contributorId":30967,"corporation":false,"usgs":true,"family":"Pollock","given":"D.W.","email":"","affiliations":[],"preferred":false,"id":370733,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70015374,"text":"70015374 - 1989 - Dikes, joints, and faults in the upper mantle","interactions":[],"lastModifiedDate":"2025-08-20T16:31:03.178741","indexId":"70015374","displayToPublicDate":"2003-04-11T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Dikes, joints, and faults in the upper mantle","docAbstract":"Three different types of macroscopic fractures are recognized in upper-mantle and lower-crustal xenoliths in volcanic rocks from around the world:
1. (1) joints that are tensile fractures not occupied by crystallized magma products
2. (2) dikes that are tensile fractures occupied by mafic magmas crystallized to pyroxenites, gabbros or hydrous-mineral-rich rocks,
3. (3) faults that are unfilled shear fractures with surface markings indicative of shear displacement.
In addition to intra-xenolith fractures, xenoliths commonly have polygonal or faceted shapes that represent fractures exploited during incorporation of the xenoliths into the host magma that brought them to the surface. The various types of fractures are considered to have formed in response to the pressures associated with magmatic fluids and to the ambient tectonic stress field. The presence of fracture sets and crosscutting relations indicate that both magma-filled and unfilled fractures can be contemporaneous and that the local stress field can change with time, leading to repeated episodes of fracture. These observations give insight into the nature of deep fracture processes and the importance of fluid-peridotite interactions in the mantle. We suggest that unfilled fractures were opened by volatile fluids exsolved from ascending magmas to the tops of growing dikes. These volatile fluids are important because they are of low viscosity and can rapidly transmit fluid pressure to dike and fault tips and because they lower the energy and tectonic stresses required to extend macroscopic cracks and to allow sliding on pre-existing fractures. Mantle seismicity at depths of 20-65 km beneath active volcanic centers in Hawaii corresponds to the depth interval where CO2-rich fluids are expected to be liberated from ascending basaltic magmas, suggesting that such fluids play an important role in facilitating earthquake instabilities in the presence of tectonic stresses.
Other phenomena related to the fractures include permeation of peridotite by fluid inclusions derived by degassing of magmas, partial melting of peridotite and dike rocks, and metasomatic alteration of peridotite host rock by magmas emplaced in fractures. These effects of magmatism generally reduce the bulk density of peridotite and might also reduce seismic velocities. The velocity contrasts between fractured and unfractured peridotite might be detected by seismic-velocity profiling techniques.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(89)90298-9","issn":"00401951","usgsCitation":"Wilshire, H.G., and Kirby, S.H., 1989, Dikes, joints, and faults in the upper mantle: Tectonophysics, v. 161, no. 1-2, p. 23-31, https://doi.org/10.1016/0040-1951(89)90298-9.","productDescription":"9 p.","startPage":"23","endPage":"31","costCenters":[],"links":[{"id":223763,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"161","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a019ee4b0c8380cd4fc94","contributors":{"authors":[{"text":"Wilshire, H. G.","contributorId":36125,"corporation":false,"usgs":false,"family":"Wilshire","given":"H.","middleInitial":"G.","affiliations":[],"preferred":false,"id":370786,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kirby, S. H.","contributorId":51721,"corporation":false,"usgs":true,"family":"Kirby","given":"S.","middleInitial":"H.","affiliations":[],"preferred":false,"id":370787,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":26870,"text":"wri884203 - 1989 - Appraisal of ground-water quality in the Bunker Hill Basin of San Bernardino Valley, California","interactions":[],"lastModifiedDate":"2012-02-02T00:08:28","indexId":"wri884203","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1989","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":"88-4203","title":"Appraisal of ground-water quality in the Bunker Hill Basin of San Bernardino Valley, California","docAbstract":"Water samples were collected from 47 wells and analyzed for concentration of major inorganic ions, nitrogen species, and volatile (purgeable) organic priority pollutants to assess groundwater quality in the Bunker Hill basin, California. Data were supplemented with additional analysis of nitrate, tetrachloroethylene, and trichloroethylene made by other agencies. The organic quality of groundwater in the basin generally is suitable for most uses, although fluoride concentration exceeded the California public drinking water standard of 1.4 mg/L in water from 5 of 47 wells. Nitrate (as nitrogen) concentration equaled or exceeded the public drinking water standard of 10 mg/L in water from 13 of 47 wells sampled for this study and in an additional 19 of 120 samples analyzed by other agencies. Concentration generally decreased with increasing depth below land surface. Twenty-four of the 33 volatile organic priority pollutants were detected in water from wells sampled during this study. When supplemental data from other agencies are included, tetrachloroethylene concentration exceeded the standard of 5 micrograms/L in water from 49 of 128 wells. No basinwide relation between contamination by these two chemicals and well depth or land use was discerned. A network of 11 observation wells that could be sampled twice a year would enhance the monitoring of changes groundwater quality in the Bunker Hill basin. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nCopies of this report can be purchased from U.S. Geological Survey, Books and Open-File Reports Section,","doi":"10.3133/wri884203","usgsCitation":"Duell, L., and Schroeder, R.A., 1989, Appraisal of ground-water quality in the Bunker Hill Basin of San Bernardino Valley, California: U.S. Geological Survey Water-Resources Investigations Report 88-4203, v, 69 p. :ill. ;28 cm., https://doi.org/10.3133/wri884203.","productDescription":"v, 69 p. :ill. ;28 cm.","costCenters":[],"links":[{"id":123517,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4203/report-thumb.jpg"},{"id":55760,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4203/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac6e4b07f02db67a3bb","contributors":{"authors":[{"text":"Duell, L. F. Jr.","contributorId":39009,"corporation":false,"usgs":true,"family":"Duell","given":"L. F.","suffix":"Jr.","affiliations":[],"preferred":false,"id":197159,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schroeder, R. A.","contributorId":15554,"corporation":false,"usgs":true,"family":"Schroeder","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":197158,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":20239,"text":"ofr8949 - 1989 - Biannual water-resources review, White Sands Missile Range, New Mexico, 1986 and 1987","interactions":[],"lastModifiedDate":"2012-02-02T00:07:35","indexId":"ofr8949","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1989","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":"89-49","title":"Biannual water-resources review, White Sands Missile Range, New Mexico, 1986 and 1987","docAbstract":"Hydrologic data were collected at White Sands Missile Range, New Mexico in 1986 and 1987. The total groundwater withdrawal in 1986 was 565,462,500 gal and in 1987 it was 620,492,000 gal. The total groundwater withdrawal was 110,971,300 gal less in 1986 than in 1985, but 55,029,500 gal more in 1987 than in 1986. Water samples from five Post Headquarters water supply wells were collected for chemical analysis in 1986. In 1987, water samples were collected from four test wells in the Post Headquarters area for analysis of selected volatile organic compounds. Twenty-eight water samples from wells were collected for analysis of specific conductance in 1986 and 1987. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nCopies of this report can be purchased from Books and Open-File Reports, Federal Center,","doi":"10.3133/ofr8949","usgsCitation":"Myers, R.G., and Sharp, S.C., 1989, Biannual water-resources review, White Sands Missile Range, New Mexico, 1986 and 1987: U.S. Geological Survey Open-File Report 89-49, iv, 36 p. ill., map ;28 cm., https://doi.org/10.3133/ofr8949.","productDescription":"iv, 36 p. ill., map ;28 cm.","costCenters":[],"links":[{"id":152505,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1989/0049/report-thumb.jpg"},{"id":49780,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1989/0049/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a51e4b07f02db62985d","contributors":{"authors":[{"text":"Myers, Robert G.","contributorId":99170,"corporation":false,"usgs":true,"family":"Myers","given":"Robert","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":182306,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sharp, Steven C.","contributorId":89917,"corporation":false,"usgs":true,"family":"Sharp","given":"Steven","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":182305,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":28446,"text":"wri894022 - 1989 - Inorganic and organic ground-water chemistry in the Canal Creek area of Aberdeen Proving Ground, Maryland","interactions":[],"lastModifiedDate":"2012-02-02T00:08:52","indexId":"wri894022","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1989","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":"89-4022","title":"Inorganic and organic ground-water chemistry in the Canal Creek area of Aberdeen Proving Ground, Maryland","docAbstract":"Groundwater chemical data were collected from November 1986 through April 1987 in the first phase of a 5-year study to assess the possibility of groundwater contamination in the Canal Creek area of Aberdeen Proving Ground, Maryland. Water samples were collected from 87 observation wells screened in Coastal Plain sediments; 59 samples were collected from the Canal Creek aquifer, 18 from the overlying surficial aquifer, and 10 from the lower confined aquifer. Dissolved solids, chloride, iron, manganese, fluoride, mercury, and chromium are present in concentrations that exceed the Federal maximum contaminant levels for drinking water. Elevated chloride and dissolved-solids concentrations appear to be related from contaminant plumes but also could result from brackish-water intrusion. Excessive concentrations of iron and manganese were the most extensive water quality problems found among the inorganic constituents and are derived from natural dissolution of minerals and oxide coatings in the aquifer sediments. Volatile organic compounds are present in the Canal Creek and surficial aquifers, but samples from the lower confined aquifer do not show any evidence of contamination by inorganic or organic chemicals. The volatile organic contaminants detected in the groundwater and their maximum concentrations (in micrograms/L) include 1,1,2,2- tetrachloroethane (9,000); carbon tetrachloride (480); chloroform (460); 1,1,2-trichloroethane (80); 1,2-dichloroethane (990); 1,1-dichloroethane (3.1); tetrachloroethylene (100); trichloroethylene (1,800); 1,2-trans- dichloroethylene (1,200); 1,1-dichloroethylene (4.4); vinyl chloride (140); benzene (70); and chlorobenzene (39). On the basis of information on past activities in the study area, some sources of the volatile organic compounds include: (1) decontaminants and degreasers; (2) clothing-impregnating operations; (3) the manufacture of impregnite material; (4) the manufacture of tear gas; and (5) fuels used in garages and at the air-field. The high density of most of the detected organic compounds in free-product form would have aided their movement into the aquifers by vertical sinking. The outcrop area of the upper confining unit and an area cut by a paleochannel are most susceptible to contamination because a near-surface impermeable layer is not present. (USGS)","language":"ENGLISH","publisher":"U.S. Geological Survey ;\r\nBooks and Open-File Reports [distributor],","doi":"10.3133/wri894022","usgsCitation":"Lorah, M., and Vroblesky, D., 1989, Inorganic and organic ground-water chemistry in the Canal Creek area of Aberdeen Proving Ground, Maryland: U.S. Geological Survey Water-Resources Investigations Report 89-4022, vii, 97 p. :ill., maps ;28 cm., https://doi.org/10.3133/wri894022.","productDescription":"vii, 97 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":123661,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1989/4022/report-thumb.jpg"},{"id":57246,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1989/4022/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57247,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1989/4022/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57248,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1989/4022/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":57249,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1989/4022/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49efe4b07f02db5ede2d","contributors":{"authors":[{"text":"Lorah, M.M.","contributorId":29002,"corporation":false,"usgs":true,"family":"Lorah","given":"M.M.","affiliations":[],"preferred":false,"id":199812,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Vroblesky, D.A.","contributorId":101691,"corporation":false,"usgs":true,"family":"Vroblesky","given":"D.A.","affiliations":[],"preferred":false,"id":199813,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
]}