During 2003–04 the U.S. Geological Survey, in cooperation with the Texas Water Development Board (TWDB) and the Harris-Galveston Coastal Subsidence District (HGCSD), used the previously developed Northern Gulf Coast Ground-Water Availability Modeling (NGC GAM) model to evaluate the effects of hypothetical projected withdrawals on ground-water flow in the northern part of the Gulf Coast aquifer system and land-surface subsidence in the NGC GAM model area of Texas. The Gulf Coast aquifer system comprises, from the surface, the Chicot and Evangeline aquifers, the Burkeville confining unit, the Jasper aquifer, and the Catahoula confining unit. Two withdrawal scenarios were simulated. The first scenario comprises historical withdrawals from the aquifer system for 1891–2000 and hypothetical projected withdrawals for 2001–50 compiled by the TWDB (TWDB scenario). The projected withdrawals compiled by the TWDB are based on ground-water demands estimated by regional water planning groups. The second scenario is a “merge” of the TWDB scenario with an alternate set of projected withdrawals from the Chicot and Evangeline aquifers in the Houston metropolitan area for 1995–2030 provided by the HGCSD (HGCSD scenario).
Under the TWDB scenario withdrawals from the entire system are projected to be about the same in 2050 as in 2000. The simulated potentiometric surfaces of the Chicot aquifer for 2010, 2020, 2030, 2040, and 2050 show relatively little change in configuration from the simulated 2000 potentiometric surface (maximum water-level depths in southern Harris County 150–200 feet below NGVD 29). The simulated decadal potentiometric surfaces of the Evangeline aquifer show the most change between 2000 and 2010. The area of water levels 250– 400 feet below NGVD 29 in western Harris County in 2000 shifts southeastward to southern Harris County, and water levels recover to 200–250 feet below NGVD 29 by 2010. Water levels in southern Harris County recover to 150–200 feet below NGVD 29 by 2020 and remain in that range through 2050. A relatively small cone of depression in southern Montgomery County that did not appear in the 2000 surface develops and enlarges during the projected period, with a maximum depth of 250–300 feet below NGVD 29 in 2030, 2040, and 2050. The simulated decadal potentiometric surfaces of the Jasper aquifer each have a major cone of depression centered in southern Montgomery County that was minimally developed in 2000 but reaches depths of 550–650 feet below NGVD 29 in the 2020, 2030, 2040, and 2050 surfaces. Under the TWDB scenario the percentage of withdrawals supplied by net recharge increases from 75 percent in 2000 to 87 percent in 2050, and the percentage of withdrawals supplied by storage decreases from 25 percent in 2000 to 13 percent in 2050.
Under the HGCSD scenario, withdrawals from the Chicot and Evangeline aquifers increase about 74 percent during 1995–2030; Jasper aquifer withdrawals are unchanged from those of the TWDB scenario. For the 2010, 2020, and 2030 potentiometric surfaces of the Chicot and Evangeline aquifers, the substantially greater withdrawals of the HGCSD scenario relative to those of the TWDB scenario result in progressively deeper cones of depression than those in the potentiometric surfaces associated with the TWDB scenario—for the Chicot aquifer in southern Harris County, 400–450 feet below NGVD 29 in 2030; for the Evangeline aquifer in southern Montgomery County, 700–750 feet below NGVD 29 in 2030. Although Jasper aquifer withdrawals are the same for both scenarios, the major cone of depression centered in southern Montgomery County in the 2030 potentiometric surface is 50 feet deeper at its center (600–700 feet below NGVD 29) than the cone in the 2030 surface under the TWDB scenario. Under the HGCSD scenario, the percentage of withdrawals supplied by net recharge decreases from 72 percent in 1995 to 57 percent in 2030, and the percentage of withdrawals supplied by storage increases from 28 percent in 2000 to 43 percent in 2030. About 85 percent of the increase supplied by storage is from the compaction of clay.
Land-surface subsidence in the major area of subsidence centered in Harris and Galveston Counties during 2000–50 that results from simulating the TWDB withdrawal scenario expands slightly to the west and increases in places. The maximum change occurs in the Conroe area where subsidence increases from about 4 to about 13 feet during the projected period. Land-surface subsidence in the major area of subsidence during 1995–2030 that results from simulating the HGCSD withdrawal scenario increases substantially. For example, in east-central Harris County maximum subsidence increases from about 10–11 feet in 1995 to 22 feet in 2030.
The hypothetical projected withdrawal scenarios are estimates of future withdrawals and might not represent actual future withdrawals. The simplifying assumptions that the downdip limit of freshwater flow in each hydrogeologic unit is a stable, sharp interface across which no flow occurs and that the base of the system is a no-flow boundary become less realistic and thus increase the uncertainty in results as drawdowns increase. The presence of uncertainty dictates that the results of the predictive simulations described in this report be used with caution in any decision-making process.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20055024","collaboration":"Prepared in cooperation with the Texas Water Development Board and the Harris-Galveston Coastal Subsidence District ","usgsCitation":"Kasmarek, M.C., Reece, B.D., and Houston, N.A., 2005, Evaluation of ground-water flow and land-surface subsidence caused by hypothetical withdrawals in the northern part of the Gulf Coast Aquifer system, Texas: U.S. Geological Survey Scientific Investigations Report 2005-5024, vi, 70 p., https://doi.org/10.3133/sir20055024.","productDescription":"vi, 70 p.","costCenters":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"links":[{"id":192568,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6938,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2005-5024/","linkFileType":{"id":5,"text":"html"}},{"id":341752,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2005/5024/pdf/sir2005-5024.pdf","text":"Report","size":"13.0 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"}],"country":"United States","state":"Texas","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -94.141845703125,\n 31.89621446335144\n ],\n [\n -97.734375,\n 29.76437737516313\n ],\n [\n -96.26220703125,\n 28.110748760633534\n ],\n [\n -92.867431640625,\n 30.107117887092357\n ],\n [\n -94.141845703125,\n 31.89621446335144\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fbe4b07f02db5f4990","contributors":{"authors":[{"text":"Kasmarek, Mark C. 0000-0003-2808-2506 mckasmar@usgs.gov","orcid":"https://orcid.org/0000-0003-2808-2506","contributorId":1968,"corporation":false,"usgs":true,"family":"Kasmarek","given":"Mark","email":"mckasmar@usgs.gov","middleInitial":"C.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282331,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reece, Brian D. bdreece@usgs.gov","contributorId":2129,"corporation":false,"usgs":true,"family":"Reece","given":"Brian","email":"bdreece@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":282332,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Houston, Natalie A. 0000-0002-6071-4545 nhouston@usgs.gov","orcid":"https://orcid.org/0000-0002-6071-4545","contributorId":1682,"corporation":false,"usgs":true,"family":"Houston","given":"Natalie","email":"nhouston@usgs.gov","middleInitial":"A.","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282330,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70392,"text":"ofr20051148 - 2005 - Acid-rock drainage at Skytop, Centre County, Pennsylvania, 2004","interactions":[],"lastModifiedDate":"2018-10-29T10:04:08","indexId":"ofr20051148","displayToPublicDate":"2005-04-15T00:00:00","publicationYear":"2005","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":"2005-1148","title":"Acid-rock drainage at Skytop, Centre County, Pennsylvania, 2004","docAbstract":"Recent construction for Interstate Highway 99 (I?99) exposed pyrite and associated Zn-Pb sulfide minerals beneath a >10-m thick gossan to oxidative weathering along a 40-60-m deep roadcut through a 270-m long section of the Ordovician Bald Eagle Formation at Skytop, near State College, Centre County, Pennsylvania. Nearby Zn-Pb deposits hosted in associated sandstone and limestone in Blair and Centre Counties were prospected in the past; however, these deposits generally were not viable as commercial mines. The pyritic sandstone from the roadcut was crushed and used locally as road base and fill for adjoining segments of I?99. Within months, acidic (pH<3), metal-laden seeps and runoff from the exposed cut and crushed sandstone raised concerns about surface- and ground-water contamination and prompted a halt in road construction and the beginning of costly remediation. Mineralized sandstones from the cut contain as much as 34 wt. % Fe, 28 wt. % S, 3.5 wt. % Zn, 1% wt. Pb, 88 ppm As, and 32 ppm Cd. A composite of <2 mm material sampled from the cut face contains 8.1 wt. % total sulfide S, 0.6 wt. % sulfate S, and is net acidic by acid-base accounting (net neutralization potential ?234 kg CaCO3/t). Primary sulfide minerals include pyrite, marcasite, sphalerite (2 to 12 wt. % Fe) and traces of chalcopyrite and galena. Pyrite occurs in mm- to cm-scale veinlets and disseminated grains in sandstone, as needles, and in a locally massive pyrite-cemented breccia along a fault. Inclusions (<10 ?m) of CdS and Ni-Co-As minerals in pyrite and minor amounts of Cd in sphalerite (0.1 wt. % or less) explain the primary source of trace metals in the rock and in associated secondary minerals and seepage. Wet/dry cycles associated with intermittent rainfall promoted oxidative weathering and dissolution of primary sulfides and their oxidation products. Resulting sulfate solutions evaporated during dry periods to form intermittent ?blooms? of soluble, yellow and white efflorescent sulfate salts (copiapite, melanterite, and halotrichite) on exposed rock and other surfaces. Salts coating the cut face incorporated Fe, Al, S, and minor Zn. They readily dissolved in deionized water in the laboratory to form solutions with pH <2.5, consistent with field observations. In addition to elevated dissolved Fe and sulfate concentrations (>1,000 mg/L), seep waters at the base of the cut contain >100 mg/L dissolved Zn and >1 mg/L As, Co, Cu, and Ni. Lead is relatively immobile (<10 ?g/L in seep waters). The salts sequester metals and acidity between rainfall events. Episodic salt dissolution then contributes pulses of contamination including acid to surface runoff and ground water. The Skytop experience highlights the need to understand dynamic interactions of mineralogy and hydrology in order to avoid potentially negative environmental impacts associated with excavation in sulfidic rocks.","language":"ENGLISH","doi":"10.3133/ofr20051148","usgsCitation":"Hammarstrom, J.M., Brady, K., and Cravotta, C.A., 2005, Acid-rock drainage at Skytop, Centre County, Pennsylvania, 2004 (Online Version 1.0): U.S. Geological Survey Open-File Report 2005-1148, 45 p., https://doi.org/10.3133/ofr20051148.","productDescription":"45 p.","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":192569,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6939,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1148/","linkFileType":{"id":5,"text":"html"}}],"edition":"Online Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699d86","contributors":{"authors":[{"text":"Hammarstrom, Jane M. 0000-0003-2742-3460 jhammars@usgs.gov","orcid":"https://orcid.org/0000-0003-2742-3460","contributorId":1226,"corporation":false,"usgs":true,"family":"Hammarstrom","given":"Jane","email":"jhammars@usgs.gov","middleInitial":"M.","affiliations":[{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":282333,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brady, Keith","contributorId":92764,"corporation":false,"usgs":true,"family":"Brady","given":"Keith","affiliations":[],"preferred":false,"id":282335,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cravotta, Charles A. III, 0000-0003-3116-4684 cravotta@usgs.gov","orcid":"https://orcid.org/0000-0003-3116-4684","contributorId":2193,"corporation":false,"usgs":true,"family":"Cravotta","given":"Charles","suffix":"III,","email":"cravotta@usgs.gov","middleInitial":"A.","affiliations":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"preferred":false,"id":282334,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70363,"text":"pp1701 - 2005 - Tephra layers of Blind Spring Valley and related upper Pliocene and Pleistocene tephra layers, California, Nevada, and Utah: Isotopic ages, correlation, and magnetostratigraphy","interactions":[],"lastModifiedDate":"2024-10-30T20:45:02.248751","indexId":"pp1701","displayToPublicDate":"2005-04-06T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1701","title":"Tephra layers of Blind Spring Valley and related upper Pliocene and Pleistocene tephra layers, California, Nevada, and Utah: Isotopic ages, correlation, and magnetostratigraphy","docAbstract":"Numerical ages have been determined for a stratigraphic sequence of silicic tephra layers exposed at the Cowan Pumice Mine in Blind Spring Valley, near Benton Hot Springs, east-central California, as well as at Chalk Cliffs, north of Bishop, Calif. The tephra layers at these sites were deposited after eruptions from nearby sources, most of them from near Glass Mountain, and some from unknown sources. The ages were determined primarily by the laser-fusion 40Ar/39Ar method, mostly on sanidine feldspar; two were determined by conventional K-Ar analysis on obsidian clasts.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1701","usgsCitation":"Sarna-Wojcicki, A.M., Reheis, M., Pringle, M.S., Fleck, R.J., Burbank, D., Meyer, C.E., Slate, J.L., Wan, E., Budahn, J.R., Troxel, B., and Walker, J.P., 2005, Tephra layers of Blind Spring Valley and related upper Pliocene and Pleistocene tephra layers, California, Nevada, and Utah: Isotopic ages, correlation, and magnetostratigraphy: U.S. Geological Survey Professional Paper 1701, v, 63 p., https://doi.org/10.3133/pp1701.","productDescription":"v, 63 p.","numberOfPages":"69","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":186325,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6525,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/pp1701/","linkFileType":{"id":5,"text":"html"}},{"id":463448,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_70954.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"California, Nevada, Utah","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -124.71679687499999,\n 34.016241889667015\n ],\n [\n -113.3349609375,\n 34.016241889667015\n ],\n [\n -113.3349609375,\n 39.232253141714885\n ],\n [\n -124.71679687499999,\n 39.232253141714885\n ],\n [\n -124.71679687499999,\n 34.016241889667015\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db685128","contributors":{"authors":[{"text":"Sarna-Wojcicki, Andrei M. 0000-0002-0244-9149 asarna@usgs.gov","orcid":"https://orcid.org/0000-0002-0244-9149","contributorId":1046,"corporation":false,"usgs":true,"family":"Sarna-Wojcicki","given":"Andrei","email":"asarna@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":282280,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Reheis, Marith C. 0000-0002-8359-323X","orcid":"https://orcid.org/0000-0002-8359-323X","contributorId":101244,"corporation":false,"usgs":true,"family":"Reheis","given":"Marith C.","affiliations":[],"preferred":false,"id":282289,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Pringle, Malcolm S.","contributorId":12929,"corporation":false,"usgs":true,"family":"Pringle","given":"Malcolm","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":282284,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fleck, Robert J. 0000-0002-3149-8249 fleck@usgs.gov","orcid":"https://orcid.org/0000-0002-3149-8249","contributorId":1048,"corporation":false,"usgs":true,"family":"Fleck","given":"Robert","email":"fleck@usgs.gov","middleInitial":"J.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":282281,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Burbank, Doug","contributorId":56732,"corporation":false,"usgs":true,"family":"Burbank","given":"Doug","email":"","affiliations":[],"preferred":false,"id":282287,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Meyer, Charles E.","contributorId":84007,"corporation":false,"usgs":true,"family":"Meyer","given":"Charles","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":282288,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Slate, Janet L. 0000-0002-2870-9068 jslate@usgs.gov","orcid":"https://orcid.org/0000-0002-2870-9068","contributorId":252,"corporation":false,"usgs":true,"family":"Slate","given":"Janet","email":"jslate@usgs.gov","middleInitial":"L.","affiliations":[{"id":501,"text":"Office of Science Quality and Integrity","active":true,"usgs":true}],"preferred":true,"id":282279,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Wan, Elmira 0000-0002-9255-112X ewan@usgs.gov","orcid":"https://orcid.org/0000-0002-9255-112X","contributorId":3434,"corporation":false,"usgs":true,"family":"Wan","given":"Elmira","email":"ewan@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":282283,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Budahn, James R. 0000-0001-9794-8882 jbudahn@usgs.gov","orcid":"https://orcid.org/0000-0001-9794-8882","contributorId":1175,"corporation":false,"usgs":true,"family":"Budahn","given":"James","email":"jbudahn@usgs.gov","middleInitial":"R.","affiliations":[{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":282282,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Troxel, Bennie","contributorId":41904,"corporation":false,"usgs":true,"family":"Troxel","given":"Bennie","affiliations":[],"preferred":false,"id":282285,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Walker, James P.","contributorId":55083,"corporation":false,"usgs":true,"family":"Walker","given":"James","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":282286,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":70364,"text":"ofr20051062 - 2005 - Reconnaissance gas measurements on the East Rift Zone of Kilauea Volcano, Hawai'i by Fourier transform infrared spectroscopy","interactions":[],"lastModifiedDate":"2019-05-07T09:53:01","indexId":"ofr20051062","displayToPublicDate":"2005-04-06T00:00:00","publicationYear":"2005","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":"2005-1062","title":"Reconnaissance gas measurements on the East Rift Zone of Kilauea Volcano, Hawai'i by Fourier transform infrared spectroscopy","docAbstract":"We report the results of a set of measurements of volcanic gases on two small ground level plumes in the vicinity of Pu`u `O`o cone on the middle East Rift Zone (ERZ) of Kilauea volcano, Hawai`i on 15 June 2001 using open-path Fourier transform infrared (FTIR) spectroscopy. The work was carried out as a reconnaissance survey to assess the monitoring and research value of FTIR measurements at this volcano. Despite representing emissions of residual volatiles from lava that has undergone prior degassing, the plumes contained detectable amounts of CO2, CO, SO2, HCl, HF and SiF4. Various processes, including subsurface cooling, condensation of water in the atmospheric plume, oxidation, dissolution in water, and reactions with wall rocks at plume vents affect the abundance of these gases. Low concentrations of volcanic CO2 measured against a high ambient background are not well constrained by FTIR spectroscopy. Although there appear to be some differences between these gases and Pu`u `O`o source gases, ratios of HCl/SO2, HF/SO2 and CO/SO2 determined by FTIR measurements of these two small plumes compare reasonably well with earlier published analyses of ERZ vent samples. The measurements yielded emission rate estimates of 4, 11 and 4 t d-1","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20051062","usgsCitation":"McGee, K.A., Elias, T., Sutton, A.J., Doukas, M.P., Zemek, P.G., and Gerlach, T.M., 2005, Reconnaissance gas measurements on the East Rift Zone of Kilauea Volcano, Hawai'i by Fourier transform infrared spectroscopy (Version 1.0): U.S. Geological Survey Open-File Report 2005-1062, 28 p., https://doi.org/10.3133/ofr20051062.","productDescription":"28 p.","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":186326,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6526,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1062/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Hawaii","otherGeospatial":"Kılauea volcano","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.3144073486328,\n 19.276146935787732\n ],\n [\n -155.1605987548828,\n 19.276146935787732\n ],\n [\n -155.1605987548828,\n 19.47241867420536\n ],\n [\n -155.3144073486328,\n 19.47241867420536\n ],\n [\n -155.3144073486328,\n 19.276146935787732\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a73e4b07f02db643f0e","contributors":{"authors":[{"text":"McGee, Kenneth A. kenmcgee@usgs.gov","contributorId":2135,"corporation":false,"usgs":true,"family":"McGee","given":"Kenneth","email":"kenmcgee@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":282290,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Elias, Tamar 0000-0002-9592-4518 telias@usgs.gov","orcid":"https://orcid.org/0000-0002-9592-4518","contributorId":3916,"corporation":false,"usgs":true,"family":"Elias","given":"Tamar","email":"telias@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":282292,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sutton, A. Jefferson","contributorId":47860,"corporation":false,"usgs":true,"family":"Sutton","given":"A.","email":"","middleInitial":"Jefferson","affiliations":[],"preferred":false,"id":282295,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Doukas, Michael P. mdoukas@usgs.gov","contributorId":2686,"corporation":false,"usgs":true,"family":"Doukas","given":"Michael","email":"mdoukas@usgs.gov","middleInitial":"P.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":282291,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Zemek, Peter G.","contributorId":32244,"corporation":false,"usgs":true,"family":"Zemek","given":"Peter","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":282294,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Gerlach, Terrence M.","contributorId":30246,"corporation":false,"usgs":true,"family":"Gerlach","given":"Terrence","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":282293,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":70003889,"text":"70003889 - 2005 - 87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico","interactions":[],"lastModifiedDate":"2020-08-31T16:33:06.135745","indexId":"70003889","displayToPublicDate":"2005-04-05T12:59:01","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2182,"text":"Journal of Archaeological Science","active":true,"publicationSubtype":{"id":10}},"displayTitle":"87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico","title":"87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico","docAbstract":"Previous analysis of 87Sr/86Sr ratios shows that 10th through 12th century Chaco Canyon was provisioned with plant materials that came from more than 75 km away. This includes (1) corn (Zea mays) grown on the eastern flanks of the Chuska Mountains and floodplain of the San Juan River to the west and north, and (2) spruce (Picea sp.) and fir (Abies sp.) beams from the crest of the Chuska and San Mateo Mountains to the west and south. Here, we extend 87Sr/86Sr analysis to ponderosa pine (Pinus ponderosa) prevalent in the architectural timber at three of the Chacoan great houses (Pueblo Bonito, Chetro Ketl, Pueblo del Arroyo). Like the architectural spruce and fir, much of the ponderosa matches the 87Sr/86Sr ratios of living trees in the Chuska Mountains. Many of the architectural ponderosa, however, have similar ratios to living trees in the La Plata and San Juan Mountains to the north and Lobo Mesa/Hosta Butte to the south. There are no systematic patterns in spruce/fir or ponderosa provenance by great house or time, suggesting the use of stockpiles from a few preferred sources. The multiple and distant sources for food and timber, now based on hundreds of isotopic values from modern and archeological samples, confirm conventional wisdom about the geographic scope of the larger Chacoan system. The complexity of this procurement warns against simple generalizations based on just one species, a single class of botanical artifact, or a few isotopic values.","language":"English","publisher":"Elsevier","publisherLocation":"London","doi":"10.1016/j.jas.2005.01.016","usgsCitation":"Reynolds, A.C., Betancourt, J.L., Quade, J., Patchett, P.J., Dean, J.S., and Stein, J., 2005, 87Sr/86Sr sourcing of ponderosa pine used in Anasazi great house construction at Chaco Canyon, New Mexico: Journal of Archaeological Science, v. 32, no. 7, p. 1061-1075, https://doi.org/10.1016/j.jas.2005.01.016.","productDescription":"15 p.","startPage":"1061","endPage":"1075","costCenters":[{"id":148,"text":"Branch of Regional Research-Western Region","active":false,"usgs":true}],"links":[{"id":203839,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Chaco Canyon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.01054000854491,\n 36.00786740304298\n ],\n [\n -107.85346984863281,\n 36.00786740304298\n ],\n [\n -107.85346984863281,\n 36.08448256814837\n ],\n [\n -108.01054000854491,\n 36.08448256814837\n ],\n [\n -108.01054000854491,\n 36.00786740304298\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"32","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b42e9","contributors":{"authors":[{"text":"Reynolds, Amanda C.","contributorId":71680,"corporation":false,"usgs":true,"family":"Reynolds","given":"Amanda","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":349317,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Betancourt, Julio L. 0000-0002-7165-0743 jlbetanc@usgs.gov","orcid":"https://orcid.org/0000-0002-7165-0743","contributorId":3376,"corporation":false,"usgs":true,"family":"Betancourt","given":"Julio","email":"jlbetanc@usgs.gov","middleInitial":"L.","affiliations":[{"id":554,"text":"Science and Decisions Center","active":true,"usgs":true},{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true},{"id":438,"text":"National Research Program - Western Branch","active":true,"usgs":true}],"preferred":true,"id":349315,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Quade, Jay","contributorId":104197,"corporation":false,"usgs":true,"family":"Quade","given":"Jay","email":"","affiliations":[],"preferred":false,"id":349320,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Patchett, P. Jonathan","contributorId":80225,"corporation":false,"usgs":true,"family":"Patchett","given":"P.","email":"","middleInitial":"Jonathan","affiliations":[],"preferred":false,"id":349318,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Dean, Jeffery S.","contributorId":93612,"corporation":false,"usgs":true,"family":"Dean","given":"Jeffery","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":349319,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Stein, John","contributorId":70527,"corporation":false,"usgs":true,"family":"Stein","given":"John","email":"","affiliations":[],"preferred":false,"id":349316,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":70351,"text":"ofr20051125 - 2005 - Radiochemical and chemical constituents in water from selected wells and springs from the southern boundary of the Idaho National Laboratory to the Hagerman Area, Idaho, 2003","interactions":[],"lastModifiedDate":"2012-02-02T00:13:48","indexId":"ofr20051125","displayToPublicDate":"2005-04-05T00:00:00","publicationYear":"2005","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":"2005-1125","title":"Radiochemical and chemical constituents in water from selected wells and springs from the southern boundary of the Idaho National Laboratory to the Hagerman Area, Idaho, 2003","docAbstract":"The U.S. Geological Survey and the Idaho Department of Water Resources, in cooperation with the U.S. Department of Energy, sampled water from 14 sites as part of an ongoing study to monitor the water quality of the eastern Snake River Plain aquifer between the southern boundary of the Idaho National Laboratory (INL) and the Burley-Twin Falls-Hagerman area. The State of Idaho, Department of Environmental Quality, Division of INL Oversight and Radiation Control cosampled with the U.S. Geological Survey and the Idaho Department of Water Resources and their analytical results are included in this report. The samples were collected from four domestic wells, two dairy wells, two springs, four irrigation wells, one observation well, and one stock well and analyzed for selected radiochemical and chemical constituents. Two quality-assurance samples, sequential replicates, also were collected and analyzed. \r\n\r\nNone of the concentrations of radiochemical or organic-chemical constituents exceeded the maximum contaminant levels for drinking water established by the U.S. Environmental Protection Agency. However, the concentration of one inorganic-chemical constituent, nitrate (as nitrogen), in water from site MV-43 was 20 milligrams per liter which exceeded the maximum contaminant level for that constituent. Of the radiochemical and chemical concentrations analyzed for in the replicate-sample pairs, 267 of the 270 pairs (with 95 percent confidence) were statistically equivalent.","language":"ENGLISH","doi":"10.3133/ofr20051125","usgsCitation":"Rattray, G.W., Wehnke, A.J., Hall, L.F., and Campbell, L.J., 2005, Radiochemical and chemical constituents in water from selected wells and springs from the southern boundary of the Idaho National Laboratory to the Hagerman Area, Idaho, 2003: U.S. Geological Survey Open-File Report 2005-1125, 30 p., https://doi.org/10.3133/ofr20051125.","productDescription":"30 p.","costCenters":[],"links":[{"id":185769,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":6500,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1125/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db634953","contributors":{"authors":[{"text":"Rattray, Gordon W. 0000-0002-1690-3218 grattray@usgs.gov","orcid":"https://orcid.org/0000-0002-1690-3218","contributorId":2521,"corporation":false,"usgs":true,"family":"Rattray","given":"Gordon","email":"grattray@usgs.gov","middleInitial":"W.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282249,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wehnke, Amy J. 0000-0003-1237-052X ajwehnke@usgs.gov","orcid":"https://orcid.org/0000-0003-1237-052X","contributorId":5660,"corporation":false,"usgs":true,"family":"Wehnke","given":"Amy","email":"ajwehnke@usgs.gov","middleInitial":"J.","affiliations":[{"id":343,"text":"Idaho Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282250,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hall, L. Flint","contributorId":53464,"corporation":false,"usgs":true,"family":"Hall","given":"L.","email":"","middleInitial":"Flint","affiliations":[],"preferred":false,"id":282251,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Campbell, Linford J.","contributorId":77174,"corporation":false,"usgs":true,"family":"Campbell","given":"Linford","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":282252,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70266,"text":"cir1280 - 2005 - Water resources and the urban environment, lower Charles River watershed, Massachusetts, 1630-2005","interactions":[],"lastModifiedDate":"2022-02-11T16:58:00.423862","indexId":"cir1280","displayToPublicDate":"2005-03-21T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1280","title":"Water resources and the urban environment, lower Charles River watershed, Massachusetts, 1630-2005","docAbstract":"The Charles River, one of the Nation’s most historically significant rivers, flows through the center of the Boston metropolitan region in eastern Massachusetts. The lower Charles River, downstream of the original head of tide in Watertown, was originally a productive estuary and important source of fish and shellfish for the Native Americans of the region. This portion of the river has an exceptionally long and colorful human history. In 1615, the explorer Captain John Smith gave the river its modern name, in honor of young Prince Charles of England. In 1617–18, the Native American community of the watershed was decimated by an epidemic, after having continuously occupied the area for the previous 4,000 years. In 1630, the first large group of English settlers, led by John Winthrop, set foot on the Shawmut Peninsula at the mouth of the river, and established the town of Boston. In the 1630s, the first printing press, public park, public school, and college in the English colonies were all established on the banks of the Charles River. Almost immediately, the settlers of Boston and adjacent towns also began to modify the landscape and water resources of the watershed.
Perhaps the most important type of landscape alteration in the watershed was the filling of the extensive salt marshes and tidal flats of the estuary downstream of Watertown. This landmaking activity along the lower Charles River began in the mid-1600s, and did not conclude until the 1950s. In the early 20th century, the estuary mouth was dammed, creating a freshwater basin in the lower 9.5 miles of the river. A system of parks and parkways was built along the banks of the impounded river. In addition to the mainstem river, virtually all of the remaining water resources in the watershed have also been altered. Most of the river’s tributaries, for example, were culverted, or placed into tunnels, and many of the ponds and freshwater wetlands in the watershed were filled to facilitate urban development.
One additional legacy of the river’s long human history is pollution from industry and sewage. By 1875, a total of 43 mills were operating along the lower Charles River between Watertown Dam and Boston Harbor. Thousands of gallons of untreated sewage and industrial wastewater entered the river daily through gravity drains, posing a major threat to public health. Concerted efforts to address the sewage problem began in the late 1870s. By the 1960s, the water quality of the river was significantly improved, yet still not suitable for swimming, fishing, or even boating under most conditions. In 1965, the Charles River Watershed Association was organized and the call to restore the environmental quality of the river and its parklands was heard anew. Passage of the Federal Clean Water Act in 1972 and the subsequent court-ordered reconstruction of the region’s sewage-treatment infrastructure in the 1980s and 1990s (the “Boston Harbor Cleanup”) provided additional impetus to address the river’s remaining pollution problems.
In 1995, the U.S. Environmental Protection Agency launched the Clean Charles 2005 Initiative, which brought together government agencies, private-sector institutions, and environmental organizations to focus on restoring the river to fishable and swimmable conditions by Earth Day 2005. This initiative has achieved substantial improvements in water quality; sewage discharges to the river, for example, have been largely eliminated. Nevertheless, it is now widely acknowledged that full attainment of water-quality standards will likely depend upon improved public understanding of the watershed, continued efforts to eliminate illicit sewage discharges to the river, and better management of the urban runoff that enters the river both directly and from its many tributary streams.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir1280","isbn":"0607968540","collaboration":"Prepared in cooperation with the U.S. Environmental Protection Agency and the Massachusetts Department of Environmental Protection","usgsCitation":"Weiskel, P.K., Barlow, L.K., and Smieszek, T.W., 2005, Water resources and the urban environment, lower Charles River watershed, Massachusetts, 1630-2005: U.S. Geological Survey Circular 1280, v, 46 p., https://doi.org/10.3133/cir1280.","productDescription":"v, 46 p.","costCenters":[],"links":[{"id":6959,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/circ/2005/1280/","linkFileType":{"id":5,"text":"html"}},{"id":186008,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/2005/1280/images/cover_sm.gif"},{"id":395460,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/2005/1280/pdf/cir1280.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Massachusetts","otherGeospatial":"Lower Charles River watershed","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.21578216552733,\n 42.22139878761366\n ],\n [\n -71.0321044921875,\n 42.22139878761366\n ],\n [\n -71.0321044921875,\n 42.404953126475725\n ],\n [\n -71.21578216552733,\n 42.404953126475725\n ],\n [\n -71.21578216552733,\n 42.22139878761366\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a05e4b07f02db5f8657","contributors":{"authors":[{"text":"Weiskel, Peter K. pweiskel@usgs.gov","contributorId":1099,"corporation":false,"usgs":true,"family":"Weiskel","given":"Peter","email":"pweiskel@usgs.gov","middleInitial":"K.","affiliations":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282074,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Barlow, Lora K.","contributorId":90279,"corporation":false,"usgs":true,"family":"Barlow","given":"Lora","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":282076,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Smieszek, Tomas W. 0000-0002-1361-2167","orcid":"https://orcid.org/0000-0002-1361-2167","contributorId":241661,"corporation":false,"usgs":true,"family":"Smieszek","given":"Tomas","email":"","middleInitial":"W.","affiliations":[{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":282075,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70253,"text":"sir20045197 - 2005 - Simulation of ground-water flow in the basin-fill aquifer of the Tularosa Basin, south-central New Mexico, predevelopment through 2040","interactions":[],"lastModifiedDate":"2012-02-02T00:13:52","indexId":"sir20045197","displayToPublicDate":"2005-03-20T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":334,"text":"Scientific Investigations Report","code":"SIR","onlineIssn":"2328-0328","printIssn":"2328-031X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"2004-5197","title":"Simulation of ground-water flow in the basin-fill aquifer of the Tularosa Basin, south-central New Mexico, predevelopment through 2040","docAbstract":"The hydrology of the basin-fill aquifer in the Tularosa Basin was evaluated through construction and calibration of steady-state and transient three-dimensional ground-water-flow simulations. Simulations were made using the U.S. Geological Survey finite-difference modular ground-water-flow computer software MODFLOW-96. The transient simulation covered 1948-2040. Both steady-state and transient simulations were calibrated by matching simulation output to available ground-water-level measurements. The root-mean-square error of the steady-state calibration in the well-calibrated area of the ground-water-flow simulation was 6.3 meters, and root-mean-square errors of individual transient-calibration points ranged from 0.8 to 17.0 meters. The areal distribution of water-level measurements used in the steady-state and transient calibrations restricts the well-calibrated area of the model to the eastern side of the Tularosa Basin. Water levels in the La Luz Creek subbasin area were underestimated by both the steady-state and transient models, suggesting that the hydrology of this area is not well represented in the model.\r\n\r\nAbout 143,000 cubic meters per day of recharge is estimated to enter the basin-fill aquifer from subbasins that rim the Tularosa Basin. The estimated recharge is about 4-5 percent of total precipitation in most subbasins. Approximately 88 percent of total recharge left the basin-fill aquifer as evapotranspiration under predevelopment conditions.\r\n\r\nWater levels were simulated for 1948, 1995, and 2040 under scenarios of zero and maximum return flows. Estimated return flows from municipalities were calculated on the basis of data in the Tularosa Basin Regional Water Plan for 2000-2040. Agricultural return flows were estimated primarily on the basis of ground-water-withdrawal, ground-water-depletion, surface-water-withdrawal, and surface-water-depletion data for the Tularosa Basin. The ground-water-flow simulation was sensitive to the return-flow scenario in the agricultural area near Tularosa and decreasingly sensitive to the south. Declines in simulated water levels near Tularosa between 1948 and 1995 were as large as 30 meters under the zero return-flow scenario and 15 meters under the maximum return-flow scenario. Declines in simulated water levels between 1995 and 2040 were as large as 25 meters under the zero return-flow scenario and 15 meters under the maximum return-flow scenario. Comparison of water levels measured near Tularosa in 1991 and water levels simulated under the maximum return-flow scenario for 1991 suggests that declines in simulated water levels near Tularosa may be overestimated under the zero return-flow scenario. Declines in simulated water levels near the City of Alamogordo well field between 1948 and 1995 were as large as 15 meters under the zero return-flow scenario and 10 meters under the maximum return-flow scenario. Simulated declines in water levels between 1995 and 2040 were nearly 15 meters under both return-flow scenarios assuming that all projected increases in withdrawal came from existing City of Alamogordo public-supply wells and all withdrawal from the wells came from the basin-fill aquifer. Declines in simulated water levels near the Holloman Air Force Base well fields between 1948 and 1995 and between 1995 and 2040 were less than 5 meters under both the zero and maximum return-flow scenarios. In 1995 under the zero return-flow scenario, an estimated 56,000 cubic meters of water per day was removed from aquifer storage. Of the approximately 199,000 cubic meters of water per day that left the aquifer under 1995 conditions, 40 percent left the basin-fill aquifer as ground-water withdrawal, 51 percent as evapotranspiration, 7 percent by interbasin ground-water flow into the Hueco Bolson, and 2 percent by flow into creeks and springs.\r\n\r\nGeneralized directions of ground-water flow were simulated for 1948, 1995, and 2040 for much of the eastern part of the Tularosa Basin. Localized","language":"ENGLISH","doi":"10.3133/sir20045197","usgsCitation":"Huff, G.F., 2005, Simulation of ground-water flow in the basin-fill aquifer of the Tularosa Basin, south-central New Mexico, predevelopment through 2040: U.S. Geological Survey Scientific Investigations Report 2004-5197, 108 p., https://doi.org/10.3133/sir20045197.","productDescription":"108 p.","costCenters":[],"links":[{"id":6955,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/sir2004-5197/","linkFileType":{"id":5,"text":"html"}},{"id":191416,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48cfe4b07f02db5461c7","contributors":{"authors":[{"text":"Huff, Glenn F.","contributorId":12079,"corporation":false,"usgs":true,"family":"Huff","given":"Glenn","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":282066,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70196,"text":"ofr20041222 - 2005 - Geological field trips in southern Idaho, eastern Oregon, and northern Nevada","interactions":[],"lastModifiedDate":"2023-04-28T19:49:02.954564","indexId":"ofr20041222","displayToPublicDate":"2005-03-11T00:00:00","publicationYear":"2005","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":"2004-1222","title":"Geological field trips in southern Idaho, eastern Oregon, and northern Nevada","docAbstract":"No abstract available.
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","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Coastal Classification Atlas","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20051003","usgsCitation":"Morton, R., and Peterson, R.L., 2005, Coastal classification atlas: Southeastern Louisiana coastal classification maps -- Pass Abel to East Timbalier Island: U.S. Geological Survey Open-File Report 2005-1003, HTML Document; 1 CD-ROM, https://doi.org/10.3133/ofr20051003.","productDescription":"HTML Document; 1 CD-ROM","onlineOnly":"Y","costCenters":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true}],"links":[{"id":188790,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":390618,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_70957.htm"},{"id":6248,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2005/1003/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Louisiana","otherGeospatial":"East Timbalier Island, Pass Abel","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.29525756835938,\n 29.084976575985912\n ],\n [\n -89.912109375,\n 29.084976575985912\n ],\n [\n -89.912109375,\n 29.27442054681336\n ],\n [\n -90.29525756835938,\n 29.27442054681336\n ],\n [\n -90.29525756835938,\n 29.084976575985912\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e6e4b07f02db5e73da","contributors":{"authors":[{"text":"Morton, Robert A.","contributorId":88333,"corporation":false,"usgs":true,"family":"Morton","given":"Robert A.","affiliations":[],"preferred":false,"id":281676,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Peterson, Russell L.","contributorId":55045,"corporation":false,"usgs":true,"family":"Peterson","given":"Russell","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":281675,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70217328,"text":"70217328 - 2005 - Structure and mechanics of the San Andreas–San Gregorio fault junction, San Francisco, California","interactions":[],"lastModifiedDate":"2021-01-15T21:02:57.911383","indexId":"70217328","displayToPublicDate":"2005-01-29T14:55:24","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":7143,"text":"Geochemistry, Geophysics, and Geosystems","active":true,"publicationSubtype":{"id":10}},"title":"Structure and mechanics of the San Andreas–San Gregorio fault junction, San Francisco, California","docAbstract":"[1] The right‐lateral San Gregorio and San Andreas faults meet west of the Golden Gate near San Francisco. Coincident seismic reflection and refraction profiling across the San Gregorio and San Andreas faults south of their junction shows the crust between them to have formed shallow extensional basins that are dissected by parallel strike‐slip faults. We employ a regional finite element model to investigate the long‐term consequences of the fault geometry. Over the course of 2–3 m.y. of slip on the San Andreas‐San Gregorio fault system, elongated extensional basins are predicted to form between the two faults. An additional consequence of the fault geometry is that the San Andreas fault is expected to have migrated eastward relative to the San Gregorio fault. We thus propose a model of eastward stepping right‐lateral fault formation to explain the observed multiple fault strands and depositional basins. The current manifestation of this process might be the observed transfer of slip from the San Andreas fault east to the Golden Gate fault.
","language":"English","publisher":"Wiley","doi":"10.1029/2004GC000838","usgsCitation":"Parsons, T., Bruns, T.R., and Sliter, R.W., 2005, Structure and mechanics of the San Andreas–San Gregorio fault junction, San Francisco, California: Geochemistry, Geophysics, and Geosystems, v. 6, no. 1, Q01009, 7 p., https://doi.org/10.1029/2004GC000838.","productDescription":"Q01009, 7 p.","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":477682,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1029/2004gc000838","text":"Publisher Index Page"},{"id":382236,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"San Francisco","otherGeospatial":"San Andreas-San Gregorio fault junction","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.5638198852539,\n 37.77017196507861\n ],\n [\n -122.48004913330077,\n 37.77017196507861\n ],\n [\n -122.48004913330077,\n 37.8271414168374\n ],\n [\n -122.5638198852539,\n 37.8271414168374\n ],\n [\n -122.5638198852539,\n 37.77017196507861\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"6","issue":"1","noUsgsAuthors":false,"publicationDate":"2005-01-29","publicationStatus":"PW","contributors":{"authors":[{"text":"Parsons, Tom 0000-0002-0582-4338","orcid":"https://orcid.org/0000-0002-0582-4338","contributorId":22056,"corporation":false,"usgs":true,"family":"Parsons","given":"Tom","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":808366,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bruns, Terry R.","contributorId":29420,"corporation":false,"usgs":true,"family":"Bruns","given":"Terry","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":808367,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sliter, Ray W. 0000-0003-0337-3454 rsliter@usgs.gov","orcid":"https://orcid.org/0000-0003-0337-3454","contributorId":1992,"corporation":false,"usgs":true,"family":"Sliter","given":"Ray","email":"rsliter@usgs.gov","middleInitial":"W.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":808368,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70242740,"text":"pp1688I - 2005 - High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia","interactions":[{"subject":{"id":70242740,"text":"pp1688I - 2005 - High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia","indexId":"pp1688I","publicationYear":"2005","noYear":false,"chapter":"I","title":"High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia"},"predicate":"IS_PART_OF","object":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"id":1}],"isPartOf":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"lastModifiedDate":"2023-04-14T16:14:13.83648","indexId":"pp1688I","displayToPublicDate":"2005-01-11T11:02:47","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1688","chapter":"I","title":"High-resolution seismic-reflection image of the Chesapeake Bay impact structure, NASA Langley Research Center, Hampton, Virginia","docAbstract":"A 1-kilometer-long (0.62-mile-long) seismic reflection and refraction profile collected at the National Aeronautics and Space Administration (NASA) Langley Research Center, Hampton, Va., provides a detailed image of part of the annular trough of the buried, 35-million-year-old Chesapeake Bay impact structure. This profile passes within 5 meters (m; 16.4 feet (ft)) of a 635.1-m-deep (2,083.8-ft-deep), continuously cored and geophysically logged test hole at the Langley Center (the USGS-NASA Langley corehole). High-resolution seismic reflection images (having a common-depth-point spacing of 2.5 m (8.2 ft)) of the upper 1,000 m (3,281 ft) along the seismic profile were generated by using refraction velocities and corehole sonic velocities to convert from time sections to depth sections.
Time-distance, unmigrated depth-distance, and migrated depth-distance images show lateral variations in the geologic units observed in the USGS-NASA Langley corehole. A high-amplitude reflection at 630 to 625 m (2,067 to 2,051 ft) depth on the migrated depth image correlates with the top of weathered granite (the Langley Granite) at 626.3 m (2,054.7 ft) in the Langley core. Additional high-amplitude reflections below that depth likely represent a weathering profile developed in the upper part of the granite. Diffractions on the unmigrated images suggest that the granite contains numerous inhomogeneities that may consist of mineral veins and mineralized faults and fractures, as seen in the granite cores.
Above the granite, crater unit A (minimally to moderately disturbed sands and clays of the Cretaceous Potomac Formation) is characterized by semicontinuous, horizontal and moderately inclined reflections that are broken by pervasive, subvertical, small-offset faults. Sediments of the lower beds of crater unit A below 558.1 m (1,831.0 ft) in the core have horizontal bedding and are nearly pristine. Above that depth, the upper beds of crater unit A contain thick fluidized sand intervals and fractured clay-silt beds. The contact between the granite and crater unit A is essentially horizontal on the migrated depth profile and shows minor relief produced by a few steeply dipping faults.
Above crater unit A, the lower beds of crater unit B are lithologically similar to the upper beds of crater unit A and display similar impact-generated deformation. In the migrated depth image, crater unit A and the lower beds of crater unit B are combined into one unit. A thin zone (0.3 m (1.0 ft) thick) of injected glauconitic sediment at the base of the lower beds (at 442.5 m (1,451.7 ft) depth) is the only occurrence of exotic material in the lower beds of crater unit B in the core.
The upper beds of crater unit B (above 427.7 m (1,403.3 ft) depth) are represented by discontinuous, locally weak, isolated, or inclined reflections on the migrated depth image. In the core, the upper beds of crater unit B are divided into megablocks and megablock zones that consist of fragmented sediments of the Potomac Formation. The megablocks are separated by matrix zones that consist of smaller blocks of sediments of the Potomac Formation suspended in a matrix of native disaggregated sediments of the Potomac Formation and injected, exotic disaggregated, glauconitic Upper Cretaceous and lower Tertiary marine sediments. Angular relationships and offsets of reflections across the high-relief contact between the upper beds of crater unit B and the underlying combined crater unit A and the lower beds of crater unit B suggest that the contact is a dip-slip fault locally.
Above a contact with crater unit B at a depth of 269.4 m (884.0 ft), the Exmore beds are represented by strong, continuous and discontinuous, overstepping reflections that suggest division of the Exmore into four laterally discontinuous depositional subunits. Two of these subunits are present near the Langley corehole on the seismic images and are recognized in the core (Gohn and others, this volume, chap. C). In the Langley core, the Exmore beds consist of clasts of Cretaceous and Tertiary preimpact sediments and cataclastic, shocked, pre-Mesozoic igneous rocks suspended in a matrix of calcareous, muddy, quartz-glauconite sand and granules that contains shocked quartz.
The dipping, truncated, and disrupted reflections within crater units A and B are interpreted to represent a 550-m-wide (1,805-ft-wide), stratabound collapse structure. This structure does not affect the underlying basement granite or the lower beds of crater unit A, nor does it affect the base of the Exmore beds above crater unit B. The collapse structure is not bounded laterally by major normal faults. Instead, structural displace ments appear to be distributed among abundant short, smalloffset faults and intervals of fluidized sediment. Fluidized sands above 558 m (1,831 ft) depth in crater unit A are interpreted as a low-strength zone that accommodated the widespread, latestage, gravitational collapse of the impact structure. The pro posed Langley collapse structure may be analogous to stratabound grabens in the outer zone of the Silverpit crater (North Sea).
The Exmore beds are interpreted as impact-generated, ocean-resurge deposits. The upper contact of the Exmore section is a wavy, semicontinuous reflection that may represent large bedforms produced by resurge currents or returning impact-generated tsunamis, or it may represent the unmodified blocky or hummocky top of the final Exmore debris flow. Typically continuous, nearly horizontal reflections characterize the upper Eocene to Pleistocene postimpact section of dominantly marine sediments.
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2005 - Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia","interactions":[{"subject":{"id":70242738,"text":"pp1688H - 2005 - Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia","indexId":"pp1688H","publicationYear":"2005","noYear":false,"chapter":"H","title":"Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia"},"predicate":"IS_PART_OF","object":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"id":1}],"isPartOf":{"id":69857,"text":"pp1688 - 2005 - Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys","indexId":"pp1688","publicationYear":"2005","noYear":false,"title":"Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys"},"lastModifiedDate":"2023-04-14T16:00:49.946324","indexId":"pp1688H","displayToPublicDate":"2005-01-11T10:43:56","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1688","chapter":"H","title":"Paleontology of the upper Eocene to quaternary postimpact section in the USGS-NASA Langley core, Hampton, Virginia","docAbstract":"The USGS-NASA Langley corehole was drilled in 2000 in Hampton, Va. The core serves as a benchmark for the study of calcareous nannofossils, dinoflagellates, diatoms and silico flagellates, mollusks, ostracodes, planktonic foraminifera and bolboformids, and vertebrate remains in the upper Eocene, Oligocene, Miocene, and Pliocene sediments in southeastern Virginia. These sediments were deposited after the comet or asteroid impact that produced the Chesapeake Bay impact structure.
The Chickahominy Formation was deposited rapidly in outer neritic to upper bathyal marine environments during the last 2 million years of the late Eocene. The Drummonds Corner beds are newly recognized in the Langley core. These beds appear to represent shallower water or more nearshore deposition than the underlying Chickahominy deposits. Paleontology indicates an age in the later part of the early Oligocene, with a sharp floral and faunal break between the Drummonds Corner beds and the underlying Chickahominy Formation. Late Oligocene sedimentation is represented by the Old Church Formation.
The record of early and middle Miocene deposition in the Langley core is incomplete. The Calvert Formation records brief episodes of deposition in three members, which are separated by unconformities and are called the informal Newport News beds, the Plum Point Member, and the Calvert Beach Member.
A second episode of rapid deposition at the Langley site is preserved as the upper Miocene St. Marys and Eastover Formations. The Eastover is overlain unconformably by the Yorktown Formation, which is both late early and early late Pliocene. The highest unit, the Tabb Formation (Pleistocene), was not studied paleontologically.
Continued movement along faults and fractures of the crater and nearby region may have enhanced the contributions of older material into the various units filling the Chesapeake Bay impact crater, as suggested by the conspicuous reworking of microfossils in many of the samples from the upper Eocene and younger units in the USGS-NASA Langley core.
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","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1688","usgsCitation":"Horton, J., Powars, D.S., and Gohn, G., 2005, Studies of the Chesapeake Bay impact structure: The USGS-NASA Langley corehole, Hampton, Virginia, and related coreholes and geophysical surveys (Version 1.0): U.S. Geological Survey Professional Paper 1688, 467 p., https://doi.org/10.3133/pp1688.","productDescription":"467 p.","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":6190,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/2005/1688/ak/","linkFileType":{"id":5,"text":"html"}},{"id":402076,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_75563.htm","linkFileType":{"id":5,"text":"html"}},{"id":90483,"rank":4,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1688/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":121027,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1688/report-thumb.jpg"}],"country":"United States","state":"Virginia","city":"Hampton","otherGeospatial":"Chesapeake Bay impact structure","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.48956298828125,\n 36.87302936279296\n ],\n [\n -75.89630126953125,\n 36.87302936279296\n ],\n [\n -75.89630126953125,\n 37.35924242260126\n ],\n [\n -76.48956298828125,\n 37.35924242260126\n ],\n [\n -76.48956298828125,\n 36.87302936279296\n ]\n ]\n ]\n }\n }\n ]\n}","edition":"Version 1.0","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699e5a","contributors":{"authors":[{"text":"Horton, J. 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The data are primarily from mesic, hilly and mountainous sites ranging from the westernmost tip of the Alaska Peninsula to the northern Kenai Peninsula, spanning 1,000 km on an E–W gradient and 700 km on a N–S gradient. 127 relevés from 18 sites represent the range of structural and compositional variation in the matrix of vegetation and landform diversity. Data were analyzed by multivariate and traditional Braun-Blanquet methods. One association is distinguished, Sambuco racemosi-Alnetum viridis ass. nov. with three new subassociations, oplopanacetosum horridi, typicum, and rubetosum spectabilis with the latter subdivided into four variants. These phytocoena are well-differentiated, although they form a syntaxonomical continuum. The composition and structure of these communities are described and interpreted in relation to complex environmental factors; these are analyzed using Jancey's ranking on F-values. Community composition is primarily related to elevation, longitude, soil moisture, and latitude. Phytogeographic comparison of southwestern Alaska alder communities with those elsewhere in the North Pacific suggests a close floristic relationship to those of southcentral, southeastern Alaska and coastal British Columbia, Canada. All these communities belong to the same association, while those of the eastern and southern parts of the Kamchatka Peninsula, Russia belong to a different association. Syntaxonomy of the 4 major communities is discussed. Within the Northern Hemisphere, vascular plant species of southwestern Alaska alder thickets primarily occur in East Asia and North America, 36 %; while 26 % are circumpolar, and 22 % are restricted to North America. From a latitudinal perspective, the distribution of vascular plant species within these alder thickets peaks in the high-subarctic, low-subarctic, and temperate latitudinal zones, with low representation of arctic species.
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\"}}]}","volume":"35","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ae7657e4b0abf75cf2bf37","contributors":{"authors":[{"text":"Talbot, Stephen S.","contributorId":73266,"corporation":false,"usgs":true,"family":"Talbot","given":"Stephen S.","affiliations":[],"preferred":false,"id":355658,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Talbot, Sandra L. 0000-0002-3312-7214 stalbot@usgs.gov","orcid":"https://orcid.org/0000-0002-3312-7214","contributorId":140512,"corporation":false,"usgs":true,"family":"Talbot","given":"Sandra","email":"stalbot@usgs.gov","middleInitial":"L.","affiliations":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":true,"id":355657,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Daniels, F. J. A.","contributorId":96196,"corporation":false,"usgs":true,"family":"Daniels","given":"F.","email":"","middleInitial":"J. A.","affiliations":[],"preferred":false,"id":355659,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70160107,"text":"70160107 - 2005 - Forestry practices and aquatic biodiversity: Fish","interactions":[],"lastModifiedDate":"2015-12-14T09:46:43","indexId":"70160107","displayToPublicDate":"2005-01-01T12:30:00","publicationYear":"2005","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":3,"text":"Organization Series"},"seriesTitle":{"id":221,"text":"Technical Bulletin","active":false,"publicationSubtype":{"id":3}},"seriesNumber":"908","title":"Forestry practices and aquatic biodiversity: Fish","docAbstract":"
In the Pacific Northwest, fish communities are found in a diverse array of aquatic habitats ranging from the large coastal rivers of the temperate rainforests, to the fragmented and sometimes ephemeral streams of the xeric interior basins, and high-elevation streams and lakes in the mountainous areas (Rieman et al. 2003). Only high-elevation lakes and streams isolated above barriers to fish passage remained historically devoid of fish because they were never invaded following Pleistocene glaciation (Smith 1981). Despite this widespread distribution and once great population abundances, taxonomic diversity of fishes in these forested systems is naturally lower than in aquatic habitats in the eastern U.S. (Reeves, Bisson, and Dambacher 1998).
Interactions among factors that influence species richness in aquatic systems (e.g., basin size, long-term stability of habitat, and barriers to colonization; Smith 1981) continue to influence the occurrence and persistence of fishes in these systems today. Consequently, the larger low-elevation rivers and estuaries support the greatest variety of fish species. In the high-elevation tributary streams, fish communities are less complex because these aquatic systems were less climatically and geologically stable, and fish populations were smaller and more prone to local extirpation. Furthermore, barriers to fish passage inhibited dispersal and colonization (Smith 1981). Streams in forested landscapes generally support salmon and trout, Oncorhynchus spp., whitefish Prosopium spp., sculpins Cottus spp., suckers Catostomus spp., and minnows (Cyprinidae), but in some of the colder streams, chars (e.g., Salvelinus confluentus and Salvelinus malma) and lampreys (Petromyzontidae)may also occur (Rieman et al. 2003).
Although biodiversity defined in terms of fish species richness is low in the Pacific Northwest, intraspecific variability is high, and polytypic fish species are common in the diverse aquatic habitats of the region. For example, the salmonids in the coastal rivers and streams, and the larger interconnected streams, rivers, and lakes of the interior exhibit a variety of ecotypes and migratory life histories (Healey 1986; Trotter 1989; Larson and McIntire 1993; Northcote 1997). This life-history variation appears to be associated with adaptation to spatial and temporal variation in environment (e.g., Schaffer and Elson 1975; Carl and Healey 1984; Beacham and Murray 1987), and there is some evidence of the genetic heritability of life-history traits (Carl and Healey 1984; Gharrett and Smoker 1993; Hankin, Nicholas, and Downey 1993). Persistence of any level of biological organization (e.g., life-history type, population, metapopulation, subspecies, species, community) is related to the interaction of environmental and biological components, and intraspecific diversity is a means of spreading risk (sensu den Boer 1968) of extirpation in dynamic environments (Gresswell 1999).
Unfortunately, despite the broad distribution and extensive intraspecific diversity, persistence of native fishes is uncertain in the Pacific Northwest. Many populations of anadromous salmonids, once synonymous with vigorous biological communities throughout the region, are threatened with extinction (Nehlsen, Williams, and Lichatowich 1991; Frissell 1993; Thurow, Lee, and Rieman 1997). Furthermore, over half of the native taxa in the Columbia River Basin are either listed under the Endangered Species Act, are being considered for listing, or are deemed sensitive by the management agencies (Lee et al. 1997; Thurow, Lee, and Rieman 1997). Potamodromous species like bull trout Salvelinus confluentus are estimated to occur as strong populations in less than 5% of their potential range (Rieman, Lee, and Thurow 1997). Although not currently listed under the endangered species list, the coastal cutthroat trout Oncorhynchus clarki is managed as a sensitive species in Oregon and California (Hall, Bisson, and Gresswell 1997). Native non-game fishes have rarely been monitored, but populations of species such as large-scale suckers (Catostomus macrocheilus), squawfish (Ptychocheilus umpquae), and Pacific lamprey (Lampetra tridentata) also are declining in some drainages (Oregon Department of Fish and Wildlife, unpublished data).
This study characterizes organic carbon (Corganic) and phosphorus (P) geochemistry in surface sediments of the Sacramento-San Joaquin Delta, California. Sediment cores were collected from five sites on a sample transect from the edge of the San Francisco Bay eastward to the freshwater Consumnes River. The top 8 cm of each core were analyzed (in 1-cm intervals) for Corganic, four P fractions, and redox-sensitive trace metals (uranium and manganese). Sedimentary Corganic concentrations and Corganic: P ratios, decreased, while reactive P concentrations increased moving inland in the Delta. The fraction of total P represented by organic P increased inland, while that of authigenic P was higher bayward than inland reflecting increased diagenetic alteration of organic matter toward the bayward end of the transect. The redox indicator metals are consistent with decreasing sedimentary suboxia inland. The distribution of P fractions and C:P ratios, reflect the presence of relatively labile organic matter in upstream surface sediments. Sediment C and P geochemistry is influenced by site-specific particulate organic matter sources, the sorptive power of the sedimentary material present, physical forcing, and early diagenetic transformations presumably driven by Corganic oxidation.
","language":"English","publisher":"Springer Link","doi":"10.1007/BF02732904","usgsCitation":"Nilsen, E.B., and Delaney, M.L., 2005, Factors influencing the biogeochemistry of sedimentary carbon and phosphorus in the Sacramento-San Joaquin Delta: Estuaries, v. 28, no. 5, p. 653-663, https://doi.org/10.1007/BF02732904.","productDescription":"11 p.","startPage":"653","endPage":"663","numberOfPages":"11","costCenters":[],"links":[{"id":237096,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Sacramento-San Joaquin Delta","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.31628417968749,\n 37.63163475580643\n ],\n [\n -121.14624023437499,\n 37.63163475580643\n ],\n [\n -121.14624023437499,\n 39.58875727696545\n ],\n [\n -122.31628417968749,\n 39.58875727696545\n ],\n [\n -122.31628417968749,\n 37.63163475580643\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"28","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0ecbe4b0c8380cd53622","contributors":{"authors":[{"text":"Nilsen, E. B.","contributorId":16637,"corporation":false,"usgs":true,"family":"Nilsen","given":"E.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":417129,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Delaney, M. L.","contributorId":41203,"corporation":false,"usgs":true,"family":"Delaney","given":"M.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":417130,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70028005,"text":"70028005 - 2005 - The 2003 eruption of Anatahan volcano, Commonwealth of the Northern Mariana Islands: Chronology, volcanology, and deformation","interactions":[],"lastModifiedDate":"2019-05-13T12:04:26","indexId":"70028005","displayToPublicDate":"2005-01-01T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"The 2003 eruption of Anatahan volcano, Commonwealth of the Northern Mariana Islands: Chronology, volcanology, and deformation","docAbstract":"The first historical eruption on Anatahan Island occurred on 10 May 2003 from the east crater of the volcano. The eruption was preceded by several hours of seismicity. Two and a half hours before the outbreak, the number of earthquakes surged to more than 100 events per hour. At 0730 UTC, the Washington Volcanic Ash Advisory Center issued an ash advisory. Although the eruption lasted for 3 months, the majority of erupted material was expelled during the first 2 weeks. The opening episode of the eruption resulted in a deposit of juvenile scoria and lithic clasts, the latter derived from geothermally altered colluvial fill from the vent area. The opening episode was followed by crater enlargement and deepening, which produced deposits of coarse, reddish-brown ash containing a mixture of juvenile and lithic clasts. The third episode of the eruption produced coarse ash and lapilli comprised of juvenile scoria and minor amounts of lithics. Plume heights were 4500 to 13,000 m for the initial three phases. The fourth episode, from about May 18 through early August, was characterized by smaller plume heights of 900 to 2400 m, and steam was the dominant component. Minor amounts of coarse ash and accretionary-lapilli ash comprise most of the deposits of the fourth episode, although ballistic blocks and bombs of andesite lava are also locally present. These andesite blocks were emplaced by an explosion on 14 June, which destroyed a small lava dome extruded during the first week of June. Activity waned as the summer progressed, and subsequent ash deposits accumulated in July and early August, by which time the eruption had effectively ended. In September and October, degassing and geothermal activity continued, characterized by small geysers, boiling water, and jetting steam. Noteworthy deviations from this activity were a surge event in late May–early June and the destruction of the lava dome on 14 June. We calculated on-land tephra-fall deposits to have a bulk volume of about 27.5 × 106 m3, covering an area of 40.6 km2. We determined the juvenile to lithic content of the deposits and corrected the bulk volume to a juvenile volume of 24.0 × 106 m3. We use a volume corrected density of 1.32 g/cm3 to convert the juvenile volume of 24.0 × 106 m3 to a magma volume of 13.2 × 106 m3. Using the methods of Fierstein and Nathenson (1992) [Fierstein, J., Nathenson, M., 1992. Another look at the calculation of fallout tephra volumes. Bull. Volcanology. 54, 156–167.], we computed the total eruption volume at 45.4 × 106 m3. Deformation surveys recorded large changes surrounding the east crater. The modeled volumetric change based on the surveys was 0.82 × 106 m3 of magma, which we estimate corresponds to a minimum intrusion of 10 × 106 m3 of magma which is in good agreement with our calculated on-land magma volume.
","language":"English","publisher":"Elsevier","doi":"10.1016/j.jvolgeores.2004.12.010","issn":"03770273","usgsCitation":"Trusdell, F., Moore, R.B., Sako, M., White, R., Koyanagi, S., Chong, R., and Camacho, J., 2005, The 2003 eruption of Anatahan volcano, Commonwealth of the Northern Mariana Islands: Chronology, volcanology, and deformation: Journal of Volcanology and Geothermal Research, v. 146, no. 1-3 , p. 184-207, https://doi.org/10.1016/j.jvolgeores.2004.12.010.","productDescription":"24 p.","startPage":"184","endPage":"207","numberOfPages":"24","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":210012,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/j.jvolgeores.2004.12.010"},{"id":236800,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Anatahan volcano","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 145.58876037597656,\n 16.32607016712877\n ],\n [\n 145.76934814453125,\n 16.32607016712877\n ],\n [\n 145.76934814453125,\n 16.378120933940313\n ],\n [\n 145.58876037597656,\n 16.378120933940313\n ],\n [\n 145.58876037597656,\n 16.32607016712877\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"146","issue":"1-3 ","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505ba646e4b08c986b320fed","contributors":{"authors":[{"text":"Trusdell, F. A.","contributorId":57471,"corporation":false,"usgs":true,"family":"Trusdell","given":"F. A.","affiliations":[],"preferred":false,"id":416117,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moore, R. B.","contributorId":98720,"corporation":false,"usgs":true,"family":"Moore","given":"R.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":416119,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sako, M.","contributorId":28383,"corporation":false,"usgs":true,"family":"Sako","given":"M.","affiliations":[],"preferred":false,"id":416114,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"White, R.A.","contributorId":21953,"corporation":false,"usgs":true,"family":"White","given":"R.A.","email":"","affiliations":[],"preferred":false,"id":416113,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Koyanagi, S.K.","contributorId":92858,"corporation":false,"usgs":true,"family":"Koyanagi","given":"S.K.","email":"","affiliations":[],"preferred":false,"id":416118,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Chong, R.","contributorId":38346,"corporation":false,"usgs":true,"family":"Chong","given":"R.","email":"","affiliations":[],"preferred":false,"id":416115,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Camacho, J.T.","contributorId":56432,"corporation":false,"usgs":true,"family":"Camacho","given":"J.T.","email":"","affiliations":[],"preferred":false,"id":416116,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":70029005,"text":"70029005 - 2005 - Toxic Alexandrium blooms in the western Gulf of Maine: The plume advection hypothesis revisited","interactions":[],"lastModifiedDate":"2017-10-04T18:23:31","indexId":"70029005","displayToPublicDate":"2005-01-01T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2620,"text":"Limnology and Oceanography","active":true,"publicationSubtype":{"id":10}},"title":"Toxic Alexandrium blooms in the western Gulf of Maine: The plume advection hypothesis revisited","docAbstract":"The plume advection hypothesis links blooms of the toxic dinoflagellate Alexandrium fundyense in the western Gulf of Maine (GOM) to a buoyant plume derived from river outflows. This hypothesis was examined with cruise and moored-instrument observations in 1993 when levels of paralytic shellfish poisoning (PSP) toxins were high, and in 1994 when toxicity was low. A coupled physical-biological model simulated hydrography and A. fundyense distributions. Initial A. fundyense populations were restricted to low-salinity nearshore waters near Casco Bay, but also occurred in higher salinity waters along the plume boundary. This suggests two sources of cells - those from shallow-water cyst populations and those transported to shore from offshore blooms in the eastern segment of the Maine coastal current (EMCC). Observations confirm the role of the plume in A. fundyense transport and growth. Downwelling-favorable winds in 1993 transported the plume and its cells rapidly alongshore, enhancing toxicity and propagating PSP to the south. In 1994, sustained upwelling moved the plume offshore, resulting in low toxicity in intertidal shellfish. A. fundyense blooms were likely nutrient limited, leading to low growth rates and moderate cell abundances. These observations and mechanisms were reproduced by coupled physical-biological model simulations. The plume advection hypothesis provides a viable explanation for outbreaks of PSP in the western GOM, but should be refined to include two sources for cells that populate the plume and two major pathways for transport: one within the low-salinity plume and another where A. fundyense cells originating in the EMCC are transported along the outer boundary of the plume front with the western segment of the Maine coastal current.","language":"English","publisher":"Wiley","doi":"10.4319/lo.2005.50.1.0328","issn":"00243590","usgsCitation":"Anderson, D., Keafer, B., Geyer, W., Signell, R.P., and Loder, T., 2005, Toxic Alexandrium blooms in the western Gulf of Maine: The plume advection hypothesis revisited: Limnology and Oceanography, v. 50, no. 1, p. 328-345, https://doi.org/10.4319/lo.2005.50.1.0328.","productDescription":"18 p.","startPage":"328","endPage":"345","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":477887,"rank":1,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.4319/lo.2005.50.1.0328","text":"Publisher Index Page"},{"id":236766,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Casco Bay, Gulf of Maine","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -66.104736328125,\n 43.88205730390537\n ],\n [\n -66.807861328125,\n 44.66083904265621\n ],\n [\n -67.60986328125,\n 44.5826428195842\n ],\n [\n -69.01611328125,\n 44.03232064275084\n ],\n [\n -70.037841796875,\n 43.75522505306931\n ],\n [\n -70.57617187499999,\n 43.30919109985686\n ],\n [\n -70.7958984375,\n 42.70665956351041\n ],\n [\n -69.90600585937499,\n 41.77950486590359\n ],\n [\n -66.324462890625,\n 43.16512263158296\n ],\n [\n -66.104736328125,\n 43.88205730390537\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"50","issue":"1","noUsgsAuthors":false,"publicationDate":"2005-01-19","publicationStatus":"PW","scienceBaseUri":"505bb5c4e4b08c986b3268b7","contributors":{"authors":[{"text":"Anderson, D.M.","contributorId":32294,"corporation":false,"usgs":true,"family":"Anderson","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":420913,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Keafer, B.A.","contributorId":77343,"corporation":false,"usgs":true,"family":"Keafer","given":"B.A.","affiliations":[],"preferred":false,"id":420916,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Geyer, W.R.","contributorId":62355,"corporation":false,"usgs":true,"family":"Geyer","given":"W.R.","email":"","affiliations":[],"preferred":false,"id":420914,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Signell, R. P.","contributorId":89147,"corporation":false,"usgs":true,"family":"Signell","given":"R.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":420917,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Loder, T.C.","contributorId":62817,"corporation":false,"usgs":true,"family":"Loder","given":"T.C.","email":"","affiliations":[],"preferred":false,"id":420915,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70027999,"text":"70027999 - 2005 - Natural landscape features, human-related attractants, and conflict hotspots: A spatial analysis of human-grizzly bear conflicts","interactions":[],"lastModifiedDate":"2012-03-12T17:20:55","indexId":"70027999","displayToPublicDate":"2005-01-01T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3671,"text":"Ursus","active":true,"publicationSubtype":{"id":10}},"title":"Natural landscape features, human-related attractants, and conflict hotspots: A spatial analysis of human-grizzly bear conflicts","docAbstract":"There is a long history of conflict in the western United States between humans and grizzly bears (Ursus arctos) involving agricultural attractants. However, little is known about the spatial dimensions of this conflict and the relative importance of different attractants. This study was undertaken to better understand the spatial and functional components of conflict between humans and grizzly bears on privately owned agricultural lands in Montana. Our investigations focused on spatial associations of rivers and creeks, livestock pastures, boneyards (livestock carcass dump sites), beehives, and grizzly bear habitat with reported human-grizzly bear conflicts during 1986-2001. We based our analysis on a survey of 61 of 64 livestock producers in our study in the Rocky Mountain East Front, Montana. With the assistance of livestock and honey producers, we mapped the locations of cattle and sheep pastures, boneyards, and beehives. We used density surface mapping to identify seasonal clusters of conflicts that we term conflict hotspots. Hotspots accounted for 75% of all conflicts and encompassed approximately 8% of the study area. We also differentiated chronic (4 or more years of conflicts) from non-chronic hotspots (fewer than 4 years of conflict). The 10 chronic hotpots accounted for 58% of all conflicts. Based on Monte Carlo simulations, we found that conflict locations were most strongly associated with rivers and creeks followed by sheep lambing areas and fall sheep pastures. Conflicts also were associated with cattle calving areas, spring cow-calf pastures, summer and fall cattle pastures, and boneyards. The Monte Carlo simulations indicated associations between conflict locations and unprotected beehives at specific analysis scales. Protected (fenced) beehives were less likely to experience conflicts than unprotected beehives. Conflicts occurred at a greater rate in riparian and wetland vegetation than would be expected. The majority of conflicts occurred in a small portion of the study area, where concentrations of attractants existed that overlapped with bear habitat. These hotspots should be the target of management and conservation efforts that focus on removing or protecting attractants using non-lethal techniques.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Ursus","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.2192/1537-6176(2005)016[0117:NLFHAA]2.0.CO;2","issn":"15376176","usgsCitation":"Wilson, S., Madel, M., Mattson, D., Graham, J., Burchfield, J., and Belsky, J., 2005, Natural landscape features, human-related attractants, and conflict hotspots: A spatial analysis of human-grizzly bear conflicts: Ursus, v. 16, no. 1, p. 117-129, https://doi.org/10.2192/1537-6176(2005)016[0117:NLFHAA]2.0.CO;2.","startPage":"117","endPage":"129","numberOfPages":"13","costCenters":[],"links":[{"id":237290,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":210387,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.2192/1537-6176(2005)016[0117:NLFHAA]2.0.CO;2"}],"volume":"16","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a6344e4b0c8380cd723c1","contributors":{"authors":[{"text":"Wilson, S.M.","contributorId":52731,"corporation":false,"usgs":true,"family":"Wilson","given":"S.M.","email":"","affiliations":[],"preferred":false,"id":416091,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Madel, M.J.","contributorId":33111,"corporation":false,"usgs":true,"family":"Madel","given":"M.J.","email":"","affiliations":[],"preferred":false,"id":416090,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mattson, D.J.","contributorId":57022,"corporation":false,"usgs":true,"family":"Mattson","given":"D.J.","email":"","affiliations":[],"preferred":false,"id":416092,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Graham, J.M.","contributorId":57651,"corporation":false,"usgs":true,"family":"Graham","given":"J.M.","email":"","affiliations":[],"preferred":false,"id":416093,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Burchfield, J.A.","contributorId":16638,"corporation":false,"usgs":true,"family":"Burchfield","given":"J.A.","email":"","affiliations":[],"preferred":false,"id":416088,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Belsky, J.M.","contributorId":27251,"corporation":false,"usgs":true,"family":"Belsky","given":"J.M.","email":"","affiliations":[],"preferred":false,"id":416089,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":70027986,"text":"70027986 - 2005 - Anatahan, Northern Mariana Islands: Reconnaissance geological observations during and after the volcanic crisis of spring 1990, and monitoring prior to the May 2003 eruption","interactions":[],"lastModifiedDate":"2019-05-14T08:38:24","indexId":"70027986","displayToPublicDate":"2005-01-01T00:00:00","publicationYear":"2005","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"Anatahan, Northern Mariana Islands: Reconnaissance geological observations during and after the volcanic crisis of spring 1990, and monitoring prior to the May 2003 eruption","docAbstract":"Anatahan island is 9.5 km east–west by 3.5 km north–south and truncated by an elongate caldera 5 km east–west by 2.5 km north–south. A steep-walled pit crater ∼1 km across and ∼200 m deep occupies the eastern part of the caldera. The island is the summit region of a mostly submarine stratovolcano. The oldest subaerial rocks (stage 1) are exposed low on the outer flanks and in the caldera walls. These include thick (∼10 m) and thin (2–3 m) lava flows, well-indurated tuffs, and scoria units that make up the bulk of the island. Rock compositions range from basaltic andesite to dacite, and most are plagioclase-phyric. On the steep north and south flanks of the volcano, these rocks are cut by numerous east–west-oriented, few-hundred-m-long lineaments of undetermined origin. Indurated breccias unconformably overlie scarps cut into stage 1 units low on the south flank. Intermediate-age eruptive units (stage 2) include caldera-filling lava flows and pyroclastic deposits and, on the outer flanks, vents and valley-filling lava flows. The youngest pre-2003 volcanic unit on Anatahan (stage 3) is a hydromagmatic surge and fall deposit rich in accretionary lapilli. Prior to 2003, this unit was found over almost the entire island, and in many places original depositional surfaces and outcrops could be found in high-energy environments along the coast, indicating a young (but undetermined) age. During reconnaissance visits in 1990, 1992, 1994, and 2001, geothermal activity (fumaroles as well as pits with boiling, sediment-laden pools) was observed in the southern part of the pit crater.
In March and April 1990, increased local seismicity, a large regional earthquake, and reported increased fumarolic activity in the pit crater prompted evacuation of Anatahan village, at the west end of the island. Our first field investigation took place in late April 1990 to assess the level of volcanic unrest, conduct reconnaissance geological observations, collect rock and geothermal water samples, and set up a geophysical monitoring network. Results at this time were inconclusive with respect to determining whether the activity was anomalous. Water in some of the geothermal pits within the pit crater was boiling, and pH values as low as 0.7 were recorded in the field. An electronic distance measurement (EDM) network was installed, and over a ∼1-week period, up to 9 cm of extension occurred across some lines but not others. Seismicity was characterized by intermittent local earthquakes but no sustained swarms or tremor. A brief visit in June 1990 revealed that the shallow lake near the boiling pits was gone, but activity in the pits themselves was similar to that of April 1990. Only minor extension had occurred along a single EDM line since the previous visit, and no earthquakes >M2.5 occurred during the visit.
Subsequent 1- to 2-day visits occurred in October 1990, May 1992, May 1994, and June 2001. Activity within the geothermal pits was relatively constant during every visit, although during this 11-year period the level of the water in each pit decreased. In June 2001, a ∼50-m-wide region of mud pots and steaming ground in the central part of the geothermal area had developed. No geologic evidence, however, suggested that an eruption would occur < 2 years afterward. Most of the EDM lines showed slight extension between late 1990 and 1992, followed by very gradual contraction from 1992 to 2001. A more extensive seismic-monitoring system was installed on the Northern Mariana Islands during these visits, and it recorded a small seismic swarm at Anatahan from May to July 1993. The telemetry component of the seismic equipment broke prior to 2001 and had not been repaired by the time of the May 2003 eruption, so no precursory seismic data were recorded to indicate pre-eruption unrest.
","language":"English","publisher":"Elsevier","doi":"10.1016/j.jvolgeores.2004.10.020","issn":"03770273","usgsCitation":"Rowland, S., Lockwood, J.P., Trusdell, F., Moore, R.B., Sako, M., Koyanagi, R.Y., and Kojima, G., 2005, Anatahan, Northern Mariana Islands: Reconnaissance geological observations during and after the volcanic crisis of spring 1990, and monitoring prior to the May 2003 eruption: Journal of Volcanology and Geothermal Research, v. 146, no. 1-3 SPEC. ISS., p. 26-59, https://doi.org/10.1016/j.jvolgeores.2004.10.020.","productDescription":"34 p.","startPage":"26","endPage":"59","numberOfPages":"34","costCenters":[{"id":615,"text":"Volcano Hazards Program","active":true,"usgs":true}],"links":[{"id":237079,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Northern Mariana Islands","otherGeospatial":"Anatahan","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 145.6182861328125,\n 16.32672912425378\n ],\n [\n 145.74188232421875,\n 16.32672912425378\n ],\n [\n 145.74188232421875,\n 16.36889775921193\n ],\n [\n 145.6182861328125,\n 16.36889775921193\n ],\n [\n 145.6182861328125,\n 16.32672912425378\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"146","issue":"1-3 SPEC. ISS.","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059ebefe4b0c8380cd48f95","contributors":{"authors":[{"text":"Rowland, S.K.","contributorId":103855,"corporation":false,"usgs":true,"family":"Rowland","given":"S.K.","email":"","affiliations":[],"preferred":false,"id":416040,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lockwood, J. P.","contributorId":104473,"corporation":false,"usgs":true,"family":"Lockwood","given":"J.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":416041,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Trusdell, F. A.","contributorId":57471,"corporation":false,"usgs":true,"family":"Trusdell","given":"F. A.","affiliations":[],"preferred":false,"id":416038,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Moore, R. B.","contributorId":98720,"corporation":false,"usgs":true,"family":"Moore","given":"R.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":416039,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Sako, M. K.","contributorId":50152,"corporation":false,"usgs":true,"family":"Sako","given":"M. K.","affiliations":[],"preferred":false,"id":416037,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Koyanagi, R. Y.","contributorId":35719,"corporation":false,"usgs":true,"family":"Koyanagi","given":"R.","email":"","middleInitial":"Y.","affiliations":[],"preferred":false,"id":416036,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Kojima, G.","contributorId":15001,"corporation":false,"usgs":true,"family":"Kojima","given":"G.","affiliations":[],"preferred":false,"id":416035,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ]}