The Blackbird cobalt-copper (Co-Cu) district in the Salmon River Mountains of east-central Idaho occupies the central part of the Idaho cobalt belt—a northwest-elongate, 55-km-long belt of Co-Cu occurrences, hosted in grayish siliciclastic metasedimentary strata of the Lemhi subbasin (of the Mesoproterozoic Belt-Purcell Basin). The Blackbird district contains at least eight stratabound ore zones and many discordant lodes, mostly in the upper part of the banded siltite unit of the Apple Creek Formation of Yellow Lake, which generally consists of interbedded siltite and argillite. In the Blackbird mine area, argillite beds in six stratigraphic intervals are altered to biotitite containing over 75 vol% of greenish hydrothermal biotite, which is preferentially mineralized.
Past production and currently estimated resources of the Blackbird district total ~17 Mt of ore, averaging 0.74% Co, 1.4% Cu, and 1.0 ppm Au (not including downdip projections of ore zones that are open downward). A compilation of relative-age relationships and isotopic age determinations indicates that most cobalt mineralization occurred in Mesoproterozoic time, whereas most copper mineralization occurred in Cretaceous time.
Mesoproterozoic cobaltite mineralization accompanied and followed dynamothermal metamorphism and bimodal plutonism during the Middle Mesoproterozoic East Kootenay orogeny (ca. 1379–1325 Ma), and also accompanied Grenvilleage (Late Mesoproterozoic) thermal metamorphism (ca. 1200–1000 Ma). Stratabound cobaltite-biotite ore zones typically contain cobaltite1 in a matrix of biotitite ± tourmaline ± minor xenotime (ca. 1370–1320 Ma) ± minor chalcopyrite ± sparse allanite ± sparse microscopic native gold in cobaltite. Such cobaltite-biotite lodes are locally folded into tight F2 folds with axial-planar S2 cleavage and schistosity. Discordant replacement-style lodes of cobaltite2-biotite ore ± xenotime2 (ca. 1320–1270 Ma) commonly follow S2fractures and fabrics. Discordant quartz-biotite and quartz-tourmaline breccias, and veins contain cobaltite3 ± xenotime3 (ca. 1058–990 Ma).
Mesoproterozoic cobaltite deposition was followed by: (1) within-plate plutonism (530–485 Ma) and emplacement of mafic dikes (which cut cobaltite lodes but are cut by quartz-Fe-Cu-sulfide veins); (2) garnet-grade metamorphism (ca. 151–93 Ma); (3) Fe-Cu-sulfide mineralization (ca. 110–92 Ma); and (4) minor quartz ± Au-Ag ± Bi mineralization (ca. 92–83 Ma).
Cretaceous Fe-Cu-sulfide vein, breccia, and replacement-style deposits contain various combinations of chalcopyrite ± pyrrhotite ± pyrite ± cobaltian arsenopyrite (not cobaltite) ± arsenopyrite ± quartz ± siderite ± monazite (ca. 144–88 Ma but mostly 110–92 Ma) ± xenotime (104–93 Ma). Highly radiogenic Pb (in these sulfides) and Sr (in siderite) indicate that these elements resided in Mesoproterozoic source rocks until they were mobilized after ca. 100 Ma. Fe-Cu-sulfide veins, breccias, and replacement deposits appear relatively undeformed and generally lack metamorphic fabrics.
Composite Co-Cu-Au ore contains early cobaltite-biotite lodes, cut by Fe-Cu-sulfide veins and breccias, or overprinted by Fe-Cu-sulfide replacement-style deposits, and locally cut by quartz veinlets ± Au-Ag ± Bi minerals.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/2016.2522(08)","usgsCitation":"Bookstrom, A.A., Box, S.E., Cossette, P.M., Frost, T.P., Gillerman, V., King, G., and Zirakparvar, N.A., 2016, Geologic history of the Blackbird Co-Cu district in the Lemhi subbasin of the Belt-Purcell Basin: GSA Special Papers, v. 522, p. 185-219, https://doi.org/10.1130/2016.2522(08).","productDescription":"36 p. ","startPage":"185","endPage":"219","ipdsId":"IP-068425","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":488685,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1130/2016.2522(08)","text":"Publisher Index Page"},{"id":342938,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Idaho","otherGeospatial":"Lemhi Subbasin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -115.12573242187499,\n 44.327777761284416\n ],\n [\n -112.9119873046875,\n 44.327777761284416\n ],\n [\n -112.9119873046875,\n 45.75985868785574\n ],\n [\n -115.12573242187499,\n 45.75985868785574\n ],\n [\n -115.12573242187499,\n 44.327777761284416\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"522","publishingServiceCenter":{"id":14,"text":"Menlo Park PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"59536ea9e4b062508e3c7a83","contributors":{"authors":[{"text":"Bookstrom, Arthur A. 0000-0003-1336-3364 abookstrom@usgs.gov","orcid":"https://orcid.org/0000-0003-1336-3364","contributorId":1542,"corporation":false,"usgs":true,"family":"Bookstrom","given":"Arthur","email":"abookstrom@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true},{"id":5056,"text":"Office of the AD Energy and Minerals, and Environmental Health","active":true,"usgs":true}],"preferred":true,"id":700798,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Box, Stephen E. 0000-0002-5268-8375 sbox@usgs.gov","orcid":"https://orcid.org/0000-0002-5268-8375","contributorId":1843,"corporation":false,"usgs":true,"family":"Box","given":"Stephen","email":"sbox@usgs.gov","middleInitial":"E.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":700799,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Cossette, Pamela M. 0000-0002-9608-6595 pcossette@usgs.gov","orcid":"https://orcid.org/0000-0002-9608-6595","contributorId":1458,"corporation":false,"usgs":true,"family":"Cossette","given":"Pamela","email":"pcossette@usgs.gov","middleInitial":"M.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":700800,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Frost, Thomas P. 0000-0001-8348-8432 tfrost@usgs.gov","orcid":"https://orcid.org/0000-0001-8348-8432","contributorId":203,"corporation":false,"usgs":true,"family":"Frost","given":"Thomas","email":"tfrost@usgs.gov","middleInitial":"P.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":700801,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Gillerman, Virginia","contributorId":193550,"corporation":false,"usgs":false,"family":"Gillerman","given":"Virginia","affiliations":[],"preferred":false,"id":700802,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"King, George","contributorId":193551,"corporation":false,"usgs":false,"family":"King","given":"George","affiliations":[],"preferred":false,"id":700803,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Zirakparvar, N. Alex","contributorId":193552,"corporation":false,"usgs":false,"family":"Zirakparvar","given":"N.","email":"","middleInitial":"Alex","affiliations":[],"preferred":false,"id":700804,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":70170603,"text":"ofr20161064 - 2016 - Geology of the Greenwater Range, and the dawn of Death Valley, California—Field guide for the Death Valley Natural History Conference, 2013","interactions":[],"lastModifiedDate":"2016-05-03T09:24:16","indexId":"ofr20161064","displayToPublicDate":"2016-05-02T17:00:00","publicationYear":"2016","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":"2016-1064","title":"Geology of the Greenwater Range, and the dawn of Death Valley, California—Field guide for the Death Valley Natural History Conference, 2013","docAbstract":"Much has been written about the age and formation of Death Valley, but that is one—if not the last—chapter in the fascinating geologic history of this area. Igneous and sedimentary rocks in the Greenwater Range, one mountain range east of Death Valley, tell an earlier story that overlaps with the formation of Death Valley proper. This early story has been told by scientists who have studied these rocks for many years and continue to do so. This field guide was prepared for the first Death Valley Natural History Conference and provides an overview of the geology of the Greenwater Range and the early history (10–0 Ma) of Death Valley.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20161064","usgsCitation":"Calzia, J.P., Rämö, O.T., Jachens, Robert, Smith, Eugene, and Knott, Jeffrey, 2016, Geology of the Greenwater Range, and the dawn of Death Valley, California—Field guide for the Death Valley Natural History Conference, 2013: U.S. Geological Survey Open-File Report 2016–1064, 32 p., https://dx.doi.org/10.3133/ofr20161064.","productDescription":"iv, 32 p.","numberOfPages":"37","onlineOnly":"Y","additionalOnlineFiles":"N","ipdsId":"IP-073504","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":320772,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2016/1064/ofr20161064.pdf","text":"Report","size":"5.8 MB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 2016-1064 Report PDF"},{"id":320771,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2016/1064/coverthb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Death Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.10052490234375,\n 36.07241230197147\n ],\n [\n -117.10052490234375,\n 36.59127365634205\n ],\n [\n -116.27517700195312,\n 36.59127365634205\n ],\n [\n -116.27517700195312,\n 36.07241230197147\n ],\n [\n -117.10052490234375,\n 36.07241230197147\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"GMEG staff, Geology, Minerals, Energy, & Geophysics Science Center—
Menlo Park, California
U.S. Geological Survey
345 Middlefield Road
Menlo Park, CA 94025-3591
http://geomaps.wr.usgs.gov/gmeg/
The occurrence of coesite in suevites from the Chesapeake Bay impact structure is confirmed within a variety of textural domains in situ by Raman spectroscopy for the first time and in mechanically separated grains by X-ray diffraction. Microtextures of coesite identified in situ investigated under transmitted light and by scanning electron microscope reveal coesite as micrometer-sized grains (1–3 μm) within amorphous silica of impact-melt clasts and as submicrometer-sized grains and polycrystalline aggregates within shocked quartz grains. Coesite-bearing quartz grains are present both idiomorphically with original grain margins intact and as highly strained grains that underwent shock-produced plastic deformation. Coesite commonly occurs in plastically deformed quartz grains within domains that appear brown (toasted) in transmitted light and rarely within quartz of spheroidal texture. The coesite likely developed by a mechanism of solid-state transformation from precursor quartz. Raman spectroscopy also showed a series of unidentified peaks associated with shocked quartz grains that likely represent unidentified silica phases, possibly including a moganite-like phase that has not previously been associated with coesite.
","language":"English","publisher":"Wiley","doi":"10.1111/maps.12638","usgsCitation":"Jackson, J.C., Horton, J.W., Chou, I., and Belkin, H.E., 2016, Coesite in suevites from the Chesapeake Bay impact structure: Meteoritics and Planetary Science, v. 51, no. 5, p. 946-965, https://doi.org/10.1111/maps.12638.","productDescription":"20 p.","startPage":"946","endPage":"965","ipdsId":"IP-065888","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"links":[{"id":346318,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Chesapeake Bay","volume":"51","issue":"5","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationDate":"2016-03-24","publicationStatus":"PW","scienceBaseUri":"59d35028e4b05fe04cc34d62","contributors":{"authors":[{"text":"Jackson, John C. jjackson@usgs.gov","contributorId":2652,"corporation":false,"usgs":true,"family":"Jackson","given":"John","email":"jjackson@usgs.gov","middleInitial":"C.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":711703,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Horton, J. Wright Jr. 0000-0001-6756-6365 whorton@usgs.gov","orcid":"https://orcid.org/0000-0001-6756-6365","contributorId":173694,"corporation":false,"usgs":true,"family":"Horton","given":"J.","suffix":"Jr.","email":"whorton@usgs.gov","middleInitial":"Wright","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":false,"id":711704,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Chou, I-Ming 0000-0001-5233-6479 imchou@usgs.gov","orcid":"https://orcid.org/0000-0001-5233-6479","contributorId":882,"corporation":false,"usgs":true,"family":"Chou","given":"I-Ming","email":"imchou@usgs.gov","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":711705,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Belkin, Harvey E. 0000-0001-7879-6529 hbelkin@usgs.gov","orcid":"https://orcid.org/0000-0001-7879-6529","contributorId":581,"corporation":false,"usgs":true,"family":"Belkin","given":"Harvey","email":"hbelkin@usgs.gov","middleInitial":"E.","affiliations":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":711706,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70184218,"text":"70184218 - 2016 - Megafloods and Clovis cache at Wenatchee, Washington","interactions":[],"lastModifiedDate":"2017-03-06T11:23:52","indexId":"70184218","displayToPublicDate":"2016-05-01T00:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3218,"text":"Quaternary Research","active":true,"publicationSubtype":{"id":10}},"title":"Megafloods and Clovis cache at Wenatchee, Washington","docAbstract":"Immense late Wisconsin floods from glacial Lake Missoula drowned the Wenatchee reach of Washington's Columbia valley by different routes. The earliest debacles, nearly 19,000 cal yr BP, raged 335 m deep down the Columbia and built high Pangborn bar at Wenatchee. As advancing ice blocked the northwest of Columbia valley, several giant floods descended Moses Coulee and backflooded up the Columbia past Wenatchee. Ice then blocked Moses Coulee, and Grand Coulee to Quincy basin became the westmost floodway. From Quincy basin many Missoula floods backflowed 50 km upvalley to Wenatchee 18,000 to 15,500 years ago. Receding ice dammed glacial Lake Columbia centuries more—till it burst about 15,000 years ago. After Glacier Peak ashfall about 13,600 years ago, smaller great flood(s) swept down the Columbia from glacial Lake Kootenay in British Columbia. The East Wenatchee cache of huge fluted Clovis points had been laid atop Pangborn bar after the Glacier Peak ashfall, then buried by loess. Clovis people came five and a half millennia after the early gigantic Missoula floods, two and a half millennia after the last small Missoula flood, and two millennia after the glacial Lake Columbia flood. People likely saw outburst flood(s) from glacial Lake Kootenay.
","language":"English","publisher":"Cambridge University Press","doi":"10.1016/j.yqres.2016.02.007","usgsCitation":"Waitt, R.B., 2016, Megafloods and Clovis cache at Wenatchee, Washington: Quaternary Research, v. 85, no. 3, p. 430-444, https://doi.org/10.1016/j.yqres.2016.02.007.","productDescription":"15 p.","startPage":"430","endPage":"444","ipdsId":"IP-022694","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":336869,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","volume":"85","issue":"3","publishingServiceCenter":{"id":14,"text":"Menlo Park PSC"},"noUsgsAuthors":false,"publicationDate":"2017-01-20","publicationStatus":"PW","scienceBaseUri":"58be8338e4b014cc3a3a99e1","contributors":{"authors":[{"text":"Waitt, Richard B. 0000-0002-6392-5604 waitt@usgs.gov","orcid":"https://orcid.org/0000-0002-6392-5604","contributorId":2343,"corporation":false,"usgs":true,"family":"Waitt","given":"Richard","email":"waitt@usgs.gov","middleInitial":"B.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":680593,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70159049,"text":"70159049 - 2016 - Estimating forest and woodland aboveground biomass using active and passive remote sensing","interactions":[],"lastModifiedDate":"2016-06-01T13:43:53","indexId":"70159049","displayToPublicDate":"2016-05-01T00:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3052,"text":"Photogrammetric Engineering and Remote Sensing","active":true,"publicationSubtype":{"id":10}},"title":"Estimating forest and woodland aboveground biomass using active and passive remote sensing","docAbstract":"Aboveground biomass was estimated from active and passive remote sensing sources, including airborne lidar and Landsat-8 satellites, in an eastern Arizona (USA) study area comprised of forest and woodland ecosystems. Compared to field measurements, airborne lidar enabled direct estimation of individual tree height with a slope of 0.98 (R2 = 0.98). At the plot-level, lidar-derived height and intensity metrics provided the most robust estimate for aboveground biomass, producing dominant species-based aboveground models with errors ranging from 4 to 14Mg ha –1 across all woodland and forest species. Landsat-8 imagery produced dominant species-based aboveground biomass models with errors ranging from 10 to 28 Mg ha –1. Thus, airborne lidar allowed for estimates for fine-scale aboveground biomass mapping with low uncertainty, while Landsat-8 seems best suited for broader spatial scale products such as a national biomass essential climate variable (ECV) based on land cover types for the United States.
","language":"English","publisher":"Ingenta","doi":"10.14358/PERS.82.4.271","usgsCitation":"Wu, Z., Dye, D.G., Vogel, J.M., and Middleton, B.R., 2016, Estimating forest and woodland aboveground biomass using active and passive remote sensing: Photogrammetric Engineering and Remote Sensing, v. 82, no. 4, p. 271-281, https://doi.org/10.14358/PERS.82.4.271.","productDescription":"11 p.","startPage":"271","endPage":"281","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-058621","costCenters":[{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"links":[{"id":471037,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.14358/pers.82.4.271","text":"Publisher Index Page"},{"id":322022,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"82","issue":"4","publishingServiceCenter":{"id":14,"text":"Menlo Park PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57500761e4b0ee97d51bb5ca","contributors":{"authors":[{"text":"Wu, Zhuoting 0000-0001-7393-1832 zwu@usgs.gov","orcid":"https://orcid.org/0000-0001-7393-1832","contributorId":4953,"corporation":false,"usgs":true,"family":"Wu","given":"Zhuoting","email":"zwu@usgs.gov","affiliations":[{"id":498,"text":"Office of Land Remote Sensing (Geography)","active":true,"usgs":true},{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":577541,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dye, Dennis G. 0000-0002-7100-272X ddye@usgs.gov","orcid":"https://orcid.org/0000-0002-7100-272X","contributorId":4233,"corporation":false,"usgs":true,"family":"Dye","given":"Dennis","email":"ddye@usgs.gov","middleInitial":"G.","affiliations":[{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":577544,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Vogel, John M. 0000-0002-8226-1188 jvogel@usgs.gov","orcid":"https://orcid.org/0000-0002-8226-1188","contributorId":3167,"corporation":false,"usgs":true,"family":"Vogel","given":"John","email":"jvogel@usgs.gov","middleInitial":"M.","affiliations":[{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":577542,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Middleton, Barry R. 0000-0001-8924-4121 bmiddleton@usgs.gov","orcid":"https://orcid.org/0000-0001-8924-4121","contributorId":3947,"corporation":false,"usgs":true,"family":"Middleton","given":"Barry","email":"bmiddleton@usgs.gov","middleInitial":"R.","affiliations":[{"id":657,"text":"Western Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":577543,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70169062,"text":"sim3351 - 2016 - Geologic map of the Valdez D-1 and D-2 quadrangles (Mount Wrangell Volcano), Alaska","interactions":[],"lastModifiedDate":"2018-06-20T19:49:59","indexId":"sim3351","displayToPublicDate":"2016-04-29T15:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":333,"text":"Scientific Investigations Map","code":"SIM","onlineIssn":"2329-132X","printIssn":"2329-1311","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"3351","title":"Geologic map of the Valdez D-1 and D-2 quadrangles (Mount Wrangell Volcano), Alaska","docAbstract":"Mount Wrangell (elev. 4,317 m) is the youngest and only active volcano in the Oligocene to Holocene-aged Wrangell volcanic field that extends from beyond the Alaska-Yukon border northwest through the Wrangell Mountains to the Copper River Basin. The volcano is a very large (900 km3) broad shield containing an ice-filled, nonexplosive, collapse caldera measuring 3.2 by 5.6 kilometers. Three known craters, the West, North, and East occur along the north and west margins of the caldera; the caldera is open to the southeast. The volcano is best exposed on its southwest flank (this map area) where a number of deep glaciated canyons cut through hundreds of meters of shield lava flows creating routes for younger, valley-filling lava flows. The shield extends north into the Gulkana A-1 quadrangle, northeast into the Nabesna A-6 quadrangle, and east into the McCarthy quadrangle where it is almost entirely covered by ice. The present extent of the Mount Wrangell shield showing the entire caldera and locations of the three summit craters is depicted in figure 1.
\nMount Wrangell was built rapidly beginning about 650 ka by the outpourings of hundreds of voluminous lava flows from a vent, or vents, apparently in the present summit area. By 200 ka to 300 ka, activity waned and only an occasional lava flow coursed down the glacially carved valleys radiating from the summit or flowed over the upper summit area above the heads of the glacial valleys. The youngest dated valley-fill lava flow is approximately 25,000 years old; one or two undated flows may be younger.
\nIn historical times there have been several reports of lava flows issuing from the summit area. The most reliable and convincing of these were two independent observations from Copper Center, Alaska on September 3, 1899 that described great earth movements (the 1899 Yakutat Bay earthquake) followed by an eruption at Mount Wrangell’s summit, consisting of vigorous ash emission and flowing lava on the volcano’s northwest flank. This eruptive activity apparently continued for several years after the earthquake, as a photo taken around 1901–02 shows a large part of Mount Wrangell’s summit blanketed by ash. During this study, no evidence of young lava flows in the region were found, although it is very possible that a small-volume flow could be entirely hidden by snow and ice in the 100 years since the event. However, abundant juvenile andesitic pumice was found on the upper Chetaslina Glacier, strongly supporting a very young pyroclastic eruption.
\nIn addition to the 1899–1902 eruptions there have been accounts of strong ash-producing activity on at least four different occasions: 1912, July 3, 1921, April 6, 1930, and February 20, 1982. Of these, the 1921 activity was the most spectacular, and possibly erupted from the northeast side of the summit caldera.
\nPresent activity is limited to fumaroles in North and West Crater at the summit, at the summit ridge near East Crater, and at two localities at an elevation of 3,657 m on the southwest flank. The summit fumaroles frequently give rise to visible steam plumes, and occasionally sporadic explosive phreatic activity in North and West Crater will put a thin dusting of ash on the summit ice.
\nThis study was directed toward Mount Wrangell volcano and the older Wrangell volcanic field rocks that underlie the volcano. These older lavas include the Chetaslina lavas (867 ka–1,650 ka) and a basaltic andesite–dacite center (1,590 ka–1,640 ka) whose source areas are not well defined. Older Paleozoic and Mesozoic sedimentary, igneous, and metamorphic rocks of the Wrangellia terrane underlie the entire Wrangell volcanic field.
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As a Federal science agency within the Department of the Interior, the U.S. Geological Survey (USGS) collects and disseminates streamflow stage and discharge information along with other types of water information as a major part of its Water mission area. Data collected at USGS streamflow-gaging stations (hereinafter referred to as “streamgages”) are used for a variety of purposes including flood warning, engineering design, management of water resources, and scientific research.
During flood events, the need for timely, accurate, and complete streamflow data is underscored because these data are relied on by local, State, and Federal emergency management personnel for flood response purposes. For example, the National Weather Service uses the data from USGS streamgages to develop flood forecasts for specific locations on a river. Tasks that the USGS performs in response to floods include monitoring the operation of gages and responding to any interruptions in data collection, calibrating and verifying stage-discharge ratings, and documenting extreme events including peak stage and peak discharge.
Frequent, severe storms during May and June 2015 caused widespread flooding in Texas. By various measures, the storms that caused the flooding were extreme and persistent. May 2015 was the wettest month on record for Texas, with a statewide average precipitation of 9.06 inches. In comparison, the long-term statewide average monthly precipitation is 3.37 inches, with the previous record average monthly precipitation reported as 6.66 inches during June 2004. The Office of the Texas State Climatologist compiled monthly precipitation amounts for 19 selected cities throughout Texas and for 1 city in Louisiana; the total monthly precipitation amounts exceeded the monthly normal precipitation for 18 of the 19 selected cities in Texas, with 5 of these cities exceeding their previous record for the month of May.
The onset of abundant precipitation in May 2015 resulted in the National Weather Service flood stage being exceeded at USGS streamgages on numerous rivers. The widespread and prolonged nature of the flooding was unusual; most flood events in Texas are localized, typically affecting only one or two river basins and generally lasting only a few days. With the exception of the Rio Grande, flooding was widespread in all of the major rivers in Texas during May–June 2015.
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\"}}]}","contact":"Director, Texas Water Science Center
U.S. Geological Survey
1505 Ferguson Lane
Austin, TX 78754–4733
Hardwood forests of eastern North America have experienced decades of acidic deposition, leading to soil acidification where base cation supply was insufficient to neutralize acid inputs. Negative impacts of soil acidity on amphibians include disrupted embryonic development, lower growth rates, and habitat loss. However, some amphibians exhibit intraspecific variation in acid tolerance, suggesting the potential for local adaptation in areas where soils are naturally acidic. The eastern red-backed salamander (Plethodon cinereus) is a highly abundant top predator of the northern hardwood forest floor. Early research found that P. cinereus was sensitive to acidic soils, avoiding substrates with pH < 3.8 and experiencing decreased growth rates in acidic habitats. However, recent studies have documented P. cinereus populations in lower pH conditions than previously observed, suggesting some populations may persist in acidic conditions. Here, we evaluated relationships between organic horizon soil pH and P. cinereus abundance, adult health (body size and condition), and microhabitat selection, based on surveys of 34 hardwood forests in northeastern United States that encompass a regional soil pH gradient. We found no associations between soil pH and P. cinereus abundance or health, and observed that this salamander used substrates with pH similar to that available, suggesting that pH does not mediate their fine-scale distributions. The strongest negative predictor of P. cinereus abundance was the presence of dusky salamanders (Desmognathus spp.), which were most abundant in the western Adirondacks. Our results indicate that P. cinereus occupies a wider range of soil pH than has been previously thought, which has implications for their functional role in forest food webs and nutrient cycles in acid-impaired ecosystems. Tolerance of P. cinereus for more acidic habitats, including anthropogenically acidified forests, may be due to local adaptation in reproductively isolated populations and/or generalist life history traits that allow them to exploit a wider resource niche.
","language":"English","publisher":"Ecological Society of America","publisherLocation":"Washington, DC","doi":"10.1002/ecs2.1318","usgsCitation":"Bondi, C.A., Beier, C.M., Ducey, P.K., Lawrence, G.B., and Bailey, S.W., 2016, Can the eastern red-backed salamander (Plethodon cinereus) persist in an acidified landscape?: Ecosphere, v. 7, no. 4, e01318, 15 p., https://doi.org/10.1002/ecs2.1318.","productDescription":"e01318, 15 p.","numberOfPages":"15","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-065102","costCenters":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"links":[{"id":471051,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1002/ecs2.1318","text":"Publisher Index Page"},{"id":320413,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.2783203125,\n 42.867912483915305\n ],\n [\n -75.2783203125,\n 44.97645666320777\n ],\n [\n -70.9716796875,\n 44.97645666320777\n ],\n [\n -70.9716796875,\n 42.867912483915305\n ],\n [\n -75.2783203125,\n 42.867912483915305\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"7","issue":"4","publishingServiceCenter":{"id":11,"text":"Pembroke PSC"},"noUsgsAuthors":false,"publicationDate":"2016-04-22","publicationStatus":"PW","scienceBaseUri":"571b3d19e4b071321fe26eb3","contributors":{"authors":[{"text":"Bondi, Cheryl A","contributorId":168843,"corporation":false,"usgs":false,"family":"Bondi","given":"Cheryl","email":"","middleInitial":"A","affiliations":[{"id":25369,"text":"SUNY Environmental Science and Forestry","active":true,"usgs":false}],"preferred":false,"id":627460,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Beier, Colin M.","contributorId":17107,"corporation":false,"usgs":true,"family":"Beier","given":"Colin","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":627461,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ducey, Peter K","contributorId":168844,"corporation":false,"usgs":false,"family":"Ducey","given":"Peter","email":"","middleInitial":"K","affiliations":[{"id":25370,"text":"SUNY Cortland","active":true,"usgs":false}],"preferred":false,"id":627462,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Lawrence, Gregory B. 0000-0002-8035-2350 glawrenc@usgs.gov","orcid":"https://orcid.org/0000-0002-8035-2350","contributorId":867,"corporation":false,"usgs":true,"family":"Lawrence","given":"Gregory","email":"glawrenc@usgs.gov","middleInitial":"B.","affiliations":[{"id":474,"text":"New York Water Science Center","active":true,"usgs":true}],"preferred":true,"id":627459,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Bailey, Scott W. 0000-0002-9160-156X","orcid":"https://orcid.org/0000-0002-9160-156X","contributorId":36840,"corporation":false,"usgs":true,"family":"Bailey","given":"Scott","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":627463,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70173814,"text":"70173814 - 2016 - The structure of genetic diversity in eelgrass (Zostera marina L.) along the North Pacific and Bering Sea coasts of Alaska","interactions":[],"lastModifiedDate":"2018-08-19T10:07:55","indexId":"70173814","displayToPublicDate":"2016-04-22T00:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2980,"text":"PLoS ONE","active":true,"publicationSubtype":{"id":10}},"displayTitle":"The structure of genetic diversity in eelgrass (Zostera marina L.) along the North Pacific and Bering Sea coasts of Alaska","title":"The structure of genetic diversity in eelgrass (Zostera marina L.) along the North Pacific and Bering Sea coasts of Alaska","docAbstract":"Eelgrass (Zostera marina) populations occupying coastal waters of Alaska are separated by a peninsula and island archipelago into two Large Marine Ecosystems (LMEs). From populations in both LMEs, we characterize genetic diversity, population structure, and polarity in gene flow using nuclear microsatellite fragment and chloroplast and nuclear sequence data. An inverse relationship between genetic diversity and latitude was observed (heterozygosity: R2 = 0.738, P < 0.001; allelic richness: R2 = 0.327, P = 0.047), as was significant genetic partitioning across most sampling sites (θ = 0.302, P < 0.0001). Variance in allele frequency was significantly partitioned by region only in cases when a population geographically in the Gulf of Alaska LME (Kinzarof Lagoon) was instead included with populations in the Eastern Bering Sea LME (θp = 0.128–0.172; P < 0.003), suggesting gene flow between the two LMEs in this region. Gene flow among locales was rarely symmetrical, with notable exceptions generally following net coastal ocean current direction. Genetic data failed to support recent proposals that multiple Zostera species (i.e. Z. japonica and Z. angustifolia) are codistributed with Z. marina in Alaska. Comparative analyses also failed to support the hypothesis that eelgrass populations in the North Atlantic derived from eelgrass retained in northeastern Pacific Last Glacial Maximum refugia. These data suggest northeastern Pacific populations are derived from populations expanding northward from temperate populations following climate amelioration at the terminus of the last Pleistocene glaciation.
","language":"English","publisher":"Public Library of Science","doi":"10.1371/journal.pone.0152701","usgsCitation":"Talbot, S.L., Sage, G.K., Rearick, J.R., Fowler, M., Muñiz-Salazar, R., Baibak, B., Wyllie-Echeverria, S., Cabello-Pasini, A., and Ward, D.H., 2016, The structure of genetic diversity in eelgrass (Zostera marina L.) along the North Pacific and Bering Sea coasts of Alaska: PLoS ONE, v. 11, no. 4, Article e0152701; 31 p., https://doi.org/10.1371/journal.pone.0152701.","productDescription":"Article e0152701; 31 p.","onlineOnly":"Y","additionalOnlineFiles":"N","ipdsId":"IP-061219","costCenters":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"links":[{"id":471053,"rank":1,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1371/journal.pone.0152701","text":"Publisher Index Page"},{"id":438617,"rank":0,"type":{"id":30,"text":"Data Release"},"url":"https://doi.org/10.5066/F7GQ6VTK","text":"USGS data release","linkHelpText":"Eelgrass (Zostera marina) Microsatellite DNA Data; Pacific Coast of North America, 2000-2009"},{"id":323474,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Bering Sea, Gulf of Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -169.013671875,\n 65.25670649344259\n ],\n [\n -179.033203125,\n 62.34960927573045\n ],\n [\n -172.08984375,\n 55.42901345240742\n ],\n [\n -177.01171875,\n 55.07836723201515\n ],\n [\n -184.04296875,\n 57.468589192089325\n ],\n [\n -183.603515625,\n 55.32914440840507\n ],\n [\n -185.361328125,\n 51.17934297928927\n ],\n [\n -178.857421875,\n 48.864714761802794\n ],\n [\n -158.55468749999997,\n 52.5897007687178\n ],\n [\n -132.451171875,\n 50.56928286558243\n ],\n [\n 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ksage@usgs.gov","orcid":"https://orcid.org/0000-0003-1431-2286","contributorId":87833,"corporation":false,"usgs":true,"family":"Sage","given":"George","email":"ksage@usgs.gov","middleInitial":"K.","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":false,"id":638486,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rearick, Jolene R. 0000-0003-0942-8268 jrearick@usgs.gov","orcid":"https://orcid.org/0000-0003-0942-8268","contributorId":195245,"corporation":false,"usgs":true,"family":"Rearick","given":"Jolene","email":"jrearick@usgs.gov","middleInitial":"R.","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":true,"id":638487,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fowler, Megan C. 0000-0002-4947-0236 mfowler@usgs.gov","orcid":"https://orcid.org/0000-0002-4947-0236","contributorId":200478,"corporation":false,"usgs":false,"family":"Fowler","given":"Megan C.","email":"mfowler@usgs.gov","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":false,"id":638488,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Muñiz-Salazar, Raquel","contributorId":171744,"corporation":false,"usgs":false,"family":"Muñiz-Salazar","given":"Raquel","affiliations":[{"id":26937,"text":"Escuela de Ciencias de la Salid, Universidad Autónoma de Baja California","active":true,"usgs":false}],"preferred":false,"id":638489,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Baibak, Bethany","contributorId":171745,"corporation":false,"usgs":false,"family":"Baibak","given":"Bethany","email":"","affiliations":[{"id":7067,"text":"Humboldt State 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dward@usgs.gov","orcid":"https://orcid.org/0000-0002-5242-2526","contributorId":3247,"corporation":false,"usgs":true,"family":"Ward","given":"David","email":"dward@usgs.gov","middleInitial":"H.","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true},{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"preferred":true,"id":638493,"contributorType":{"id":1,"text":"Authors"},"rank":9}]}} ,{"id":70169104,"text":"sir20165031 - 2016 - The source of groundwater and solutes to Many Devils Wash at a former uranium mill site in Shiprock, New Mexico","interactions":[],"lastModifiedDate":"2016-04-25T09:52:57","indexId":"sir20165031","displayToPublicDate":"2016-04-21T17:15:00","publicationYear":"2016","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":"2016-5031","title":"The source of groundwater and solutes to Many Devils Wash at a former uranium mill site in Shiprock, New Mexico","docAbstract":"The Shiprock Disposal Site is the location of the former Navajo Mill (Mill), a uranium ore-processing facility, located on a terrace overlooking the San Juan River in the town of Shiprock, New Mexico. Following the closure of the Mill, all tailings and associated materials were encapsulated in a disposal cell built on top of the former Mill and tailings piles. The milling operations, conducted at the site from 1954 to 1968, created radioactive tailings and process-related wastes that are now found in the groundwater. Elevated concentrations of constituents of concern—ammonium, manganese, nitrate, selenium, strontium, sulfate, and uranium—have also been measured in groundwater seeps in the nearby Many Devils Wash arroyo, leading to the inference that these constituents originated from the Mill. These constituents have also been reported in groundwater that is associated with Mancos Shale, the bedrock that underlies the site. The objective of this report is to increase understanding of the source of water and solutes to the groundwater beneath Many Devils Wash and to establish the background concentrations for groundwater that is in contact with the Mancos Shale at the site. This report presents evidence on three working hypotheses: (1) the water and solutes in Many Devils Wash originated from the operations at the former Mill, (2) groundwater in deep aquifers is upwelling under artesian pressure to recharge the shallow groundwater beneath Many Devils Wash, and (3) the groundwater beneath Many Devils Wash originates as precipitation that infiltrates into the shallow aquifer system and discharges to Many Devils Wash in a series of springs on the east side of the wash. The solute concentrations in the shallow groundwater of Many Devils Wash would result from the interaction of the water and the Mancos Shale if the source of water was upwelling from deep aquifers or precipitation.
In order to compare the groundwater from various wells to groundwater that has been affected by Mill activities, a classification system was developed to determine which wells were most likely to have been affected. Affects to groundwater by the Mill were determined by using the reported uranium alpha activity ratios measured in groundwater samples, along with the concentration of the uranium and the location of the wells relative to the Mill. Activity ratios of 1.2 or less were determined to be the most reliable indicator of Mill-affected groundwater. Wells with samples that had a reported activity ratio of 1.2 or less were classified as Mill affected. To compare groundwater with background water-quality, data from groundwater seeps and springs in the Upper Eagle Nest Arroyo and Salt Creek Wash, located north of the San Juan River, are also presented and analyzed.
Based on groundwater elevations and tritium concentrations measured in wells located between the disposal cell and Many Devils Wash, Mill water is not likely to reach Many Devils Wash. The tritium concentrations also indicate that groundwater from the Mill has not substantially affected Many Devils Wash in the past. Upwelling from deep aquifers was also determined to be an unlikely source, primarily by comparing the composition of the stable isotopes of water in the shallow groundwater with those reported in groundwater samples from the deeper aquifers. The stable-isotope compositions of the shallow groundwater around the site are enriched relative to the San Juan River and local meteoric lines, which suggests that most of the shallow groundwater has been influenced by evaporation and therefore was recharged at the surface. Several observations indicate that focused recharge is the likely source of groundwater in the area of Many Devils Wash. The visible erosional features in Many Devils Wash provide evidence of piping and groundwater sapping, and the distribution and type of vegetation in Many Devils Wash suggest that the focused recharge of precipitation is occurring. The estimated recharge from precipitation was calculated to be 0.0008 inches per year (in/yr) by using the mass-balance approach from reported seep discharge and 0.0011 in/yr using the chloride mass-balance approach.
A conceptual model of groundwater quality beneath Many Devils Wash is presented to explain the source of solutes in the groundwater beneath Many Devils Wash. The major-ion concentrations and geochemical evolution in the groundwater beneath Many Devils Wash and across the study area support the conceptual model that the underlying Mancos Shale is the source of solutes. Differences in the major-ion composition between groundwater samples collected around the site, result from the degree of weathering to the Mancos Shale. The cation distribution appears to be an indicator of effects from the Mill, with samples from the Mill-affected wells largely having a calcium/magnesium-sulfate composition that resembles the reported compositions of more weathered shale; however, that composition could change if the Mill-processed water flowed into areas where the Mancos Shale was less weathered. On the basis of the widespread presence of uranium in the Mancos Shale and the distribution of aqueous uranium in the analog sites and other sites in the region, it appears likely that uranium in the groundwater of Many Devils Wash is naturally sourced from the Mancos Shale.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20165031","collaboration":"Prepared in cooperation with the Navajo Nation Environmental Protection Agency","usgsCitation":"Robertson, A.J., Ranalli, A.J., Austin, S.A., and Lawlis, B.R., 2016, The source of groundwater and solutes to Many Devils Wash at a former uranium mill site in Shiprock, New Mexico: U.S. Geological Survey Scientific Investigations Report 2016–5031, 54 p., https://dx.doi.org/10.3133/sir20165031.","productDescription":"x, 54 p.","onlineOnly":"Y","additionalOnlineFiles":"N","ipdsId":"IP-051391","costCenters":[{"id":472,"text":"New Mexico Water Science Center","active":true,"usgs":true}],"links":[{"id":320372,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/sir/2016/5031/coverthb.jpg"},{"id":320373,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2016/5031/sir20165031.pdf","text":"Report","size":"5.19 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIR 2016-5031"}],"country":"United States","state":"New Mexico","otherGeospatial":"Shiprock","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.74404907226562,\n 36.84775766525783\n ],\n [\n -108.74267578125,\n 36.70806354647625\n ],\n [\n -108.54766845703125,\n 36.71356812817935\n ],\n [\n -108.56552124023438,\n 36.869733528373395\n ],\n [\n -108.74542236328125,\n 36.87742358748459\n ],\n [\n -108.74404907226562,\n 36.84775766525783\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, New Mexico Water Science Center
U.S. Geological Survey
5338 Montgomery Blvd. NE
Suite 400
Albuquerque, NM 87109
http://nm.water.usgs.gov/
Concentrations of H2O and CO2 in olivine-hosted melt inclusions can be used to estimate crystallization depths for the olivine host. However, the original dissolved CO2concentration of melt inclusions at the time of trapping can be difficult to measure directly because in many cases substantial CO2 is transferred to shrinkage bubbles that form during post-entrapment cooling and crystallization. To investigate this problem, we heated olivine from the 1959 Kīlauea Iki and 1960 Kapoho (Hawai‘i) eruptions in a 1-atm furnace to temperatures above the melt inclusion trapping temperature to redissolve the CO2 in shrinkage bubbles. The measured CO2 concentrations of the experimentally rehomogenized inclusions (⩽590 ppm for Kīlauea Iki [n=10]; ⩽880 ppm for Kapoho, with one inclusion at 1863 ppm [n=38]) overlap with values for naturally quenched inclusions from the same samples, but experimentally rehomogenized inclusions have higher within-sample median CO2 values than naturally quenched inclusions, indicating at least partial dissolution of CO2 from the vapor bubble during heating. Comparison of our data with predictions from modeling of vapor bubble formation and published Raman data on the density of CO2 in the vapor bubbles suggests that 55-85% of the dissolved CO2 in the melt inclusions at the time of trapping was lost to post-entrapment shrinkage bubbles. Our results combined with the Raman data demonstrate that olivine from the early part of the Kīlauea Iki eruption crystallized at <6 km depth, with the majority of olivine in the 1-3 km depth range. These depths are consistent with the interpretation that the Kīlauea Iki magma was supplied from Kīlauea’s summit magma reservoir (∼2-5 km depth). In contrast, olivine from Kapoho, which was the rift zone extension of the Kīlauea Iki eruption, crystallized over a much wider range of depths (∼1-16 km). The wider depth range requires magma transport during the Kapoho eruption from deep beneath the summit region and/or from deep beneath Kīlauea’s east rift zone. The deeply derived olivine crystals and their host magma mixed with stored, more evolved magma in the rift zone, and the mixture was later erupted at Kapoho.
\nThe Rio Rico and Nogales (Arizona) 1:24,000-scale quadrangles are located in the Basin and Range Province of southern Arizona, and the southern edge of the map is the international border with Sonora, Mexico. The major urban area is Nogales, a bi-national city known as “the gateway to Mexico.” Rocks exposed in the map area range in age from Jurassic through Quaternary. Major physiographic, geologic, and hydrologic features in the map area include the southern San Cayetano Mountains, Grosvenor Hills, and Sonoita Creek in the northern part, and Mount Benedict and the Mount Benedict horst block in the southcentral part. The horst block is bounded by the Santa Cruz River on the east and Nogales Wash on the west.
\nThe objectives of our mapping were to define the geologic framework for the Nogales area and the upper Santa Cruz basin to support ongoing multidisciplinary projects. This new work will improve understanding of the Nogales Formation to more fully assess its groundwater resource potential. We significantly revised the Miocene Nogales Formation based on geologic mapping combined with new geochronologic, geophysical, and petrographic studies.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sim3354","usgsCitation":"Page, W.R., Menges, C.M., Gray, Floyd, Berry, M.E., Bultman, M.W., Cosca, M.A., and VanSistine, D.P., 2016, Geologic map of the Rio Rico and Nogales 7.5’ quadrangles, Santa Cruz County, Arizona: U.S. Geological Survey Scientific Investigations Map 3354, 32 p. pamphlet, 2 sheets, scale 1:24,000, https://dx.doi.org/10.3133/sim3354.","productDescription":"Pamphlet: v, 32 p.; 3 Sheets: 37.93 x 40.26 inches or smaller; Appendix; Metadata: text, xml; Read Me; Spatial Data: Base maps, Geodatabase, Shapefiles.","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-059210","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":320004,"rank":8,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_shapefiles.zip","text":"Shapefiles","size":"1.94 MB","linkFileType":{"id":6,"text":"zip"},"description":"SIM 3354 Shapefiles"},{"id":320000,"rank":6,"type":{"id":26,"text":"Sheet"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_sheet2.pdf","text":"Cross sections","size":"184 kB","linkFileType":{"id":1,"text":"pdf"},"description":"SIM 3354 Cross sections"},{"id":320006,"rank":9,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/sim/3354/sim3354.met","text":"Metadata text","size":"24.0 kB","description":"SIM 3354 Metadata Text"},{"id":319994,"rank":4,"type":{"id":26,"text":"Sheet"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_sheet1.pdf","text":"Geologic map","size":"21.4 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIM 3354 Geologic Map"},{"id":320007,"rank":10,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_basemaps.zip","text":"Base maps","size":"18.4 MB","linkFileType":{"id":6,"text":"zip"},"description":"SIM 3354 Base maps"},{"id":319992,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_pamphlet.pdf","text":"Pamphlet","size":"21.0 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIM 3354 Pamphlet"},{"id":319993,"rank":3,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_readme.txt","text":"Read Me","size":"8.0 kB","linkFileType":{"id":2,"text":"txt"},"description":"SIM 3354 ReadMe"},{"id":320009,"rank":11,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_appendix.xlsx","text":"Combined 40Ar/39Ar data","size":"68.0 kB","linkFileType":{"id":3,"text":"xlsx"},"description":"SIM 3354 Combined 40Ar/39Ar data"},{"id":320002,"rank":7,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_gdb.zip","text":"Geodatabase","size":"39.5 MB","linkFileType":{"id":6,"text":"zip"},"description":"SIM 3354 Geodatabase"},{"id":320052,"rank":12,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_metadata.xml","text":"Metadata xml","size":"20.0 kB","description":"SIM 3354 Metadata xml"},{"id":319996,"rank":5,"type":{"id":26,"text":"Sheet"},"url":"https://pubs.usgs.gov/sim/3354/sim3354_sheet1_geo.pdf","text":"Georeferenced geologic map","size":"146.0 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIM 3354 Georeferenced geologic map"},{"id":319989,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/sim/3354/coverthb.jpg"}],"country":"United States","state":"Arizona","county":"Santa Cruz County","otherGeospatial":"Rio Rico and Nogales 7.5' Quadrangles","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111,\n 31.5\n ],\n [\n -111,\n 31.3325\n ],\n [\n -110.875,\n 31.3329\n ],\n [\n -110.875,\n 31.5\n ],\n [\n -111,\n 31.5\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Center Director, USGS Geosciences and Environmental Change Science Center
Box 25046, Mail Stop 980
Denver, CO 80225
This paper represents the first attempt to show, by means other than just petrographic ones, that one type of macrinite, herein designated copromacrinite, may result from macrofauna feces. For that purpose a combination of coal petrography, X-ray photoelectron spectroscopy, and elemental-analysis continuous-flow isotope ratio mass spectrometry methods were used to determine nitrogen functionalities and δ13C andδ15N compositions in 1) vitrinite-rich, 2) fusinite + semifusinite-rich, and 3) macrinite-rich (with a possible coprolitic origin) samples of the high volatile A bituminous Peach Orchard coal (Bolsovian; Middle Pennsylvanian) from Magoffin County, Kentucky. There were no significant differences between pyridinic-N and quaternary-N abundance in the three samples, however, pyrrolic-N was higher (~ 54%) in the macrinite-rich sample than in the other two samples (~ 38%). The data suggest that pyridinic-N and quaternary-N are independent of maceral group composition and that pyrrolic-N is dependent on maceral composition (fusinite + semifusinite versus macrinite). δ13C values obtained for bulk and demineralized coal of the vitrinite- and fusinite + semifusinite-rich samples are similar with δ13C values of − 24.80 ± 0.01‰ VPDB and − 24.61 ± 0.09‰ VPDB for bulk samples and − 24.81 ± 0.07‰ VPDB and − 24.52 ± 0.04‰ VPDB for demineralized samples. These values are within the expected range for vitrinite-rich samples and the slightly higher δ13C value of the fusinite + semifusinite-rich sample is expected as δ13C values for inertinite are higher than for vitrinite. However, there was a significant shift to a lower δ13C value (− 26.80 ± 0.01‰ VPDB for the bulk sample value) for the macrinite-rich sample. Because the samples are basically isorank, and δ13C (and δ15N) shifts do not occur during maturation until anthracite rank, the difference may be related to the presence or composition of the macrinite within the sample which lacks heat-effect indicators, such as devolatilization vacuoles and distorted pores. δ15N values are also similar for bulk and demineralized coal of the vitrinite- and fusinite + semifusinite-rich samples, and the bulk values were heavier in this samples (3.07 ± 0.03‰ Air and 2.92 ± 0.10‰ Air, respectively), and much lighter (− 2.83 ± 0.09‰ Air) for the macrinite-rich sample.
\nThe study of Peach Orchard coal samples using reflected-light microscopy, isotopic composition, and nitrogen-forms analyses revealed that the macrinite-rich sample contains macrinite with coprolitic features (e.g. oxidation rind, mix of undigested palynomorphs, frequent and randomly located funginite, agglutination pulp of semifusinite reflectance, internal lack of bedding fabric, and suggestion of structures resulting from intestines and stomach walls), more pyrrolic-N (~ 16%), and lower δ13C (~ 2‰ VPDB) and δ15N (~ 4‰ Air) values than the vitrinite and semifusinite + fusinite rich samples. These findings suggest that the maceral macrinite has multiple origins based on petrography and measurable chemical differences between the macrinite, vitrinite, and semifusinite + fusinite fractions within the coal. Assuming that copromacrinite observed is an excretion then the anomalies observed may result from the symbiotic relations between the macrofauna (e.g. cockroaches) and microbiota during the digestive processes, and the nitrogen balance mechanisms inside macrofauna body.
","language":"English","publisher":"Elsevier","doi":"10.1016/j.coal.2016.05.004","usgsCitation":"Valentim, B., Algarra, M., Guedes, A., Ruppert, L.F., and Hower, J., 2016, Notes on the origin of copromacrinite based on nitrogen functionalities and δ13C and δ15N determined on samples from the Peach Orchard coal bed, southern Magoffin County, Kentucky: International Journal of Coal Geology, v. 160-161, p. 63-72, https://doi.org/10.1016/j.coal.2016.05.004.","productDescription":"10 p.","startPage":"63","endPage":"72","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-062704","costCenters":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":324653,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Kentucky","county":"Magoffin 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PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5774f2a3e4b07dd077c6a7b0","contributors":{"authors":[{"text":"Valentim, Bruno","contributorId":145465,"corporation":false,"usgs":false,"family":"Valentim","given":"Bruno","email":"","affiliations":[{"id":16122,"text":"Centro de Geologia da Universidade do Porto and Departamento de Geociências, Ambiente e Ordenamento do Território, Faculdade de Ciências da Universidade do Porto, Rua Campo Alegre, 687, 4169-007 Porto, Portugal.","active":true,"usgs":false}],"preferred":false,"id":564116,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Algarra, Manuel","contributorId":145466,"corporation":false,"usgs":false,"family":"Algarra","given":"Manuel","email":"","affiliations":[{"id":16122,"text":"Centro de Geologia da Universidade do Porto and Departamento de Geociências, Ambiente e Ordenamento do Território, Faculdade de Ciências da Universidade do Porto, Rua Campo Alegre, 687, 4169-007 Porto, Portugal.","active":true,"usgs":false}],"preferred":false,"id":564117,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Guedes, Alexandra","contributorId":145467,"corporation":false,"usgs":false,"family":"Guedes","given":"Alexandra","email":"","affiliations":[{"id":16122,"text":"Centro de Geologia da Universidade do Porto and Departamento de Geociências, Ambiente e Ordenamento do Território, Faculdade de Ciências da Universidade do Porto, Rua Campo Alegre, 687, 4169-007 Porto, Portugal.","active":true,"usgs":false}],"preferred":false,"id":564118,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ruppert, Leslie F. 0000-0002-7453-1061 lruppert@usgs.gov","orcid":"https://orcid.org/0000-0002-7453-1061","contributorId":660,"corporation":false,"usgs":true,"family":"Ruppert","given":"Leslie","email":"lruppert@usgs.gov","middleInitial":"F.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":564115,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Hower, James C. 0000-0003-4694-2776","orcid":"https://orcid.org/0000-0003-4694-2776","contributorId":34561,"corporation":false,"usgs":false,"family":"Hower","given":"James C.","affiliations":[{"id":16123,"text":"University of Kentucky, Center for Applied Energy Research, 2540 Research Park Drive, Lexington, KY 40511, United States.","active":true,"usgs":false}],"preferred":false,"id":564119,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70169095,"text":"sir20165030 - 2016 - Perchlorate and selected metals in water and soil within Mount Rushmore National Memorial, South Dakota, 2011–15","interactions":[],"lastModifiedDate":"2017-10-12T19:58:59","indexId":"sir20165030","displayToPublicDate":"2016-04-14T00:00:00","publicationYear":"2016","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":"2016-5030","title":"Perchlorate and selected metals in water and soil within Mount Rushmore National Memorial, South Dakota, 2011–15","docAbstract":"Mount Rushmore National Memorial is located in the east-central part of the Black Hills area of South Dakota and is challenged to provide drinking water to about 3 million annual visitors and year-round park personnel. An environmental concern to water resources within Mount Rushmore National Memorial has been the annual aerial fireworks display at the memorial for the Independence Day holiday during 1998–2009. A major concern of park management is the contamination of groundwater and surface water by perchlorate, which is used as an oxidizing agent in firework displays. A study by the U.S. Geological Survey, in cooperation with the National Park Service, was completed to characterize the occurrence of perchlorate and selected metals (constituents commonly associated with fireworks) in groundwater and surface water within and adjacent to Mount Rushmore National Memorial during 2011–15. Concentrations of perchlorate and metals in 106 water samples (collected from 6 groundwater sites and 14 surface-water sites) and 11 soil samples (collected from 11 soil sites) are reported.
Within the Mount Rushmore National Memorial boundary, perchlorate concentrations were greatest in the Lafferty Gulch drainage basin, ranging from less than 0.20 to 38 micrograms per liter (μg/L) in groundwater samples and from 2.2 to 54 μg/L in surface-water samples. Sites within the Starling Gulch drainage basin also had some evidence of perchlorate contamination, with concentrations ranging from 0.61 to 19 μg/L. All groundwater and surface-water samples within the unnamed tributary to Grizzly Bear Creek drainage basin and reference sites outside the park boundary had concentrations less than 0.20 μg/L. Perchlorate concentrations in samples collected at the 200-foot-deep production well (Well 1) ranged from 17 to 38 μg/L with a median of 23 μg/L, whereas perchlorate concentrations in samples from the 500-foot-deep production well (Well 2) ranged from 2.1 to 17 μg/L, with a median of 6.1 μg/L. Perchlorate concentrations in samples of the treated groundwater were similar to the concentrations from Well 1, which was the predominant source of the water supply at Mount Rushmore National Memorial during the study period (2011–15). Springflow upstream from the production wells in the West Fork Lafferty Gulch drainage had the greatest perchlorate concentrations, ranging from 21 to 54 μg/L. The groundwater site within Lafferty Gulch drainage basin but downstream from the park boundary also had a perchlorate concentration less than 0.20 μg/L in the one sample collected at the site. Water samples collected at reference sites generally had concentrations of metals within the same range of those sites within the Mount Rushmore National Memorial boundary, presenting little evidence of metal contamination due to anthropogenic factors within the park boundary. Soil samples were collected near most water sampling sites and within the Hall of Records Canyon where fireworks were launched. Perchlorate concentrations in soil were greatest in the West Fork Lafferty Gulch drainage and Hall of Records Canyon, which are topographically higher than the two groundwater wells.
The perchlorate concentrations in groundwater and surface water within Lafferty Gulch drainage basin during 2011–15 were greater than the U.S. Environmental Protection Agency’s Interim Drinking Water Health Advisory benchmark of 15 μg/L. The perchlorate concentrations in the Mount Rushmore water supply relative to this benchmark are of concern; however, this health advisory is based on the assumption that consumers are using the supply as their primary water source and currently is not a regulated standard. The groundwater system at West Fork Lafferty Gulch is highly susceptible to contamination by way of recharge and is isolated from downstream movement by an intrusive body acting as a dam, which may explain why a contamination problem is not likely to disappear or disperse, as could happen in larger aquifer systems. The observed deposition of firework debris within Lafferty Gulch drainage basin coupled with the lack of alternative perchlorate sources indicates that past firework displays are the most probable source of perchlorate contamination.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20165030","collaboration":"Prepared in cooperation with the National Park Service and National Water Quality Program–National Park Service Water Quality Partnership","usgsCitation":"Hoogestraat, G.K., and Rowe, B.L., 2016, Perchlorate and selected metals in water and soil within Mount Rushmore National Memorial, South Dakota, 2011–15: U.S. Geological Survey Scientific Investigations Report 2016–5030, 29 p., https://dx.doi.org/10.3133/sir20165030.","productDescription":"vi, 29 p.","numberOfPages":"40","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-070373","costCenters":[{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":320048,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/sir/2016/5030/coverthb.jpg"},{"id":320051,"rank":3,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2016/5030/sir20165030_appendix.xlsx","text":"Appendix 1","size":"26.4 kB","linkFileType":{"id":3,"text":"xlsx"},"description":"SIR 2016–5030 Appendix 1"},{"id":320050,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2016/5030/sir20165030.pdf","text":"Report","size":"2.59 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIR 2016–5030"}],"country":"United States","state":"South Dakota","otherGeospatial":"Mt. Rushmore","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.46129894256592,\n 43.88270687270729\n ],\n [\n -103.4487247467041,\n 43.88264500931701\n ],\n [\n -103.45160007476807,\n 43.87450941385015\n ],\n [\n -103.4608268737793,\n 43.87426192585682\n ],\n [\n -103.46275806427002,\n 43.88270687270729\n ],\n [\n -103.46129894256592,\n 43.88270687270729\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, South Dakota Water Science Center
U.S. Geological Survey
1608 Mountain View Road
Rapid City, South Dakota 57702
The state of Pennsylvania has a long history of oil and gas extraction. In recent years with advances in technology such as hydraulic fracturing, hydrocarbon sources that were not profitable in the past are now being exploited. Here, we present an assessment of the cumulative impact of oil and gas extraction activities on the forests of 35 counties in Pennsylvania and their intersecting sub-watersheds between 2004 and 2010. The assessment categorizes counties and sub-watersheds based on the estimated amount of change to forest cover in the area. From the data collected we recognize that although forest cover has not been greatly impacted (with an average loss of percent forest coverage of 0.16% at the county level), landscape structure is affected. Increase in edge forest and decrease in interior forest is evident in many of the counties and sub-watersheds examined. These changes can have a detrimental effect on forest biodiversity and dynamics.
","language":"English","publisher":"Taylor & Francis Online","doi":"10.1080/17445647.2016.1170642","usgsCitation":"Roig-Silva, C., Slonecker, E.T., Milheim, L., Ballew, J.R., and Winters, S.G., 2016, Forest cover changes due to hydrocarbon extraction disturbance in central Pennsylvania (2004–2010): Journal of Maps, v. 12, no. s1, p. 131-138, https://doi.org/10.1080/17445647.2016.1170642.","productDescription":"8 p.","startPage":"131","endPage":"138","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-066163","costCenters":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"links":[{"id":471075,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1080/17445647.2016.1170642","text":"Publisher Index Page"},{"id":320029,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Pennsylvania","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -79.541015625,\n 42.00032514831621\n ],\n [\n -80.518798828125,\n 40.9964840143779\n ],\n [\n -80.52978515625,\n 39.71986348549764\n ],\n [\n -78.057861328125,\n 39.72831341029745\n ],\n [\n -77.662353515625,\n 40.333983227838104\n ],\n [\n -77.6953125,\n 40.91766362458114\n ],\n [\n -77.025146484375,\n 41.244772343082104\n ],\n [\n -76.5582275390625,\n 41.236511201246216\n ],\n [\n -76.453857421875,\n 40.91766362458114\n ],\n [\n -75.50354003906249,\n 41.15384235711447\n ],\n [\n -74.970703125,\n 41.50857729743935\n ],\n [\n -75.1025390625,\n 41.81636125072054\n ],\n [\n -75.3717041015625,\n 42.004407212963585\n ],\n [\n -79.541015625,\n 42.00032514831621\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"12","issue":"s1","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationDate":"2016-04-13","publicationStatus":"PW","scienceBaseUri":"570f5f9ce4b0ef3b7ca32953","contributors":{"authors":[{"text":"Roig-Silva, Coral croig@usgs.gov","contributorId":168590,"corporation":false,"usgs":true,"family":"Roig-Silva","given":"Coral","email":"croig@usgs.gov","affiliations":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":626626,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Slonecker, E. Terrence 0000-0002-5793-0503 tslonecker@usgs.gov","orcid":"https://orcid.org/0000-0002-5793-0503","contributorId":168591,"corporation":false,"usgs":true,"family":"Slonecker","given":"E.","email":"tslonecker@usgs.gov","middleInitial":"Terrence","affiliations":[{"id":36171,"text":"National Civil Applications Center","active":true,"usgs":true},{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":626627,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Milheim, Lesley lmilheim@usgs.gov","contributorId":168592,"corporation":false,"usgs":true,"family":"Milheim","given":"Lesley","email":"lmilheim@usgs.gov","affiliations":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":626628,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Ballew, Jesse R. jballew@usgs.gov","contributorId":5708,"corporation":false,"usgs":true,"family":"Ballew","given":"Jesse","email":"jballew@usgs.gov","middleInitial":"R.","affiliations":[],"preferred":true,"id":626629,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Winters, S. Gail gwinters@usgs.gov","contributorId":5528,"corporation":false,"usgs":true,"family":"Winters","given":"S.","email":"gwinters@usgs.gov","middleInitial":"Gail","affiliations":[{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":626630,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70175004,"text":"70175004 - 2016 - Proposed Auxiliary Boundary Stratigraphic Section and Point (ASSP) for the base of the Ordovician System at Lawson Cove, Utah, USA","interactions":[],"lastModifiedDate":"2016-07-27T09:27:41","indexId":"70175004","displayToPublicDate":"2016-04-13T14:30:00","publicationYear":"2016","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3481,"text":"Stratigraphy","active":true,"publicationSubtype":{"id":10}},"title":"Proposed Auxiliary Boundary Stratigraphic Section and Point (ASSP) for the base of the Ordovician System at Lawson Cove, Utah, USA","docAbstract":"The Global boundary Stratotype Section and Point (GSSP) for the base of the Ordovician System is at the First Appearance Datum (FAD) of the conodont Iapetognathus fluctivagus at Green Point in Newfoundland, Canada. Strata there are typical graptolitic facies that were deposited near the base of the continental slope.We propose establishing an Auxiliary boundary Stratotype Section and Point (ASSP) at the FAD of I. fluctivagus at the Lawson Cove section in the Ibex area of Millard County, Utah, USA. There, strata consist of typical shelly facies limestones that were deposited on a tropical carbonate platform and contain abundant conodonts, trilobites, brachiopods, and other fossil groups. Cambrian and Ordovician strata in this area are ~5300m thick, with the Lawson Cove section spanning 243m in three overlapping segments. Six other measured and studied sections in the area show stratigraphic relationships similar to those at Lawson Cove. Faunas have been used to divide these strata into 14 conodont and 7 trilobite zonal units. The widespread olenid trilobite Jujuyaspis occurs ~90cm above the proposed boundary at Lawson Cove; this genus is generally regarded as earliest Ordovician. Rhynchonelliform and linguliform brachiopods are common to abundant and are useful for correlation. The FAD of Iapetognathus fluctivagus and occurrences of Jujuyaspis and the Lower Ordovician planktonic graptolite Anisograptus matanensis all occur within a 2.4m interval of strata at a nearby section. Non-biological correlation tools include a detailed sequence stratigraphic classification and a detailed carbon-isotope profile. Especially useful for correlation is a positive \u000213C excursion peak ~15cm below the proposed boundary horizon. All of these correlation tools form an integrated framework that makes the Lawson Cove section especially useful as an ASSP for global correlation of strata with faunas typical of shallow, warm-water, shelly facies.
","language":"English","publisher":"Micropaleontology Press","usgsCitation":"Miller, J.F., Evans, K.R., Ethington, R.L., Freeman, R., Loch, J.D., Repetski, J.E., Ripperdan, R., and Taylor, J.F., 2016, Proposed Auxiliary Boundary Stratigraphic Section and Point (ASSP) for the base of the Ordovician System at Lawson Cove, Utah, USA: Stratigraphy, v. 12, no. 3 - 4, p. 219-236.","productDescription":"18 p.","startPage":"219","endPage":"236","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-068560","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":325692,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":325691,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.micropress.org/microaccess/stratigraphy"}],"country":"United 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\"}}]}","volume":"12","issue":"3 - 4","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5799db6ae4b0589fa1c7ea23","contributors":{"authors":[{"text":"Miller, James F.","contributorId":147224,"corporation":false,"usgs":false,"family":"Miller","given":"James","email":"","middleInitial":"F.","affiliations":[{"id":16806,"text":"Missouri State University","active":true,"usgs":false}],"preferred":false,"id":643572,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Evans, Kevin R.","contributorId":35724,"corporation":false,"usgs":true,"family":"Evans","given":"Kevin","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":643573,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ethington, Raymond L.","contributorId":93507,"corporation":false,"usgs":false,"family":"Ethington","given":"Raymond","email":"","middleInitial":"L.","affiliations":[{"id":6754,"text":"University of 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USA","interactions":[],"lastModifiedDate":"2016-04-13T09:28:25","indexId":"70170227","displayToPublicDate":"2016-04-13T00:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":666,"text":"Aeolian Research","active":true,"publicationSubtype":{"id":10}},"title":"Geochemical evidence for seasonal controls on the transportation of Holocene loess, Matanuska Valley, southern Alaska, USA","docAbstract":"Loess is a widespread Quaternary deposit in Alaska and loess accretion occurs today in some regions, such as the Matanuska Valley. The source of loess in the Matanuska Valley has been debated for more than seven decades, with the Knik River and the Matanuska River, both to the east, being the leading candidates and the Susitna River, to the west, as a less favorable source. We report here new stratigraphic, mineralogic, and geochemical data that test the competing hypotheses of these river sources. Loess thickness data are consistent with previous studies that show that a source or sources lay to the east, which rules out the Susitna River as a source. Knik and Matanuska River silts can be distinguished using Sc–Th–La, LaN/YbN vs. Eu/Eu∗, Cr/Sc, and As/Sb. Matanuska Valley loess falls clearly within the range of values for these ratios found in Matanuska River silt. Dust storms from the Matanuska River are most common in autumn, when river discharge is at a minimum and silt-rich point bars are exposed, wind speed from the north is beginning to increase after a low-velocity period in summer, snow depth is still minimal, and soil temperatures are still above freezing. Thus, seasonal changes in climate and hydrology emerge as critical factors in the timing of aeolian silt transport in southern Alaska. These findings could be applicable to understanding seasonal controls on Pleistocene loess accretion in Europe, New Zealand, South America, and elsewhere in North America.
","language":"English","publisher":"Elsevier Science","doi":"10.1016/j.aeolia.2016.02.005","usgsCitation":"Muhs, D., Budahn, J.R., Skipp, G.L., and McGeehin, J., 2016, Geochemical evidence for seasonal controls on the transportation of Holocene loess, Matanuska Valley, southern Alaska, USA: Aeolian Research, v. 21, p. 61-73, https://doi.org/10.1016/j.aeolia.2016.02.005.","productDescription":"13 p.","startPage":"61","endPage":"73","ipdsId":"IP-068983","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":471077,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1016/j.aeolia.2016.02.005","text":"Publisher Index Page"},{"id":320018,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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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":626545,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Skipp, Gary L. 0000-0002-9404-0980 gskipp@usgs.gov","orcid":"https://orcid.org/0000-0002-9404-0980","contributorId":2102,"corporation":false,"usgs":true,"family":"Skipp","given":"Gary","email":"gskipp@usgs.gov","middleInitial":"L.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":626546,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"McGeehin, John mcgeehin@usgs.gov","contributorId":167455,"corporation":false,"usgs":true,"family":"McGeehin","given":"John","email":"mcgeehin@usgs.gov","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":242,"text":"Eastern Geographic Science Center","active":true,"usgs":true}],"preferred":true,"id":626547,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70164456,"text":"sir20165012 - 2016 - Variability in rainfall at monitoring stations and derivation of a long-term rainfall intensity record in the Grand Canyon Region, Arizona, USA","interactions":[],"lastModifiedDate":"2016-04-12T09:26:18","indexId":"sir20165012","displayToPublicDate":"2016-04-11T15:00:00","publicationYear":"2016","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":"2016-5012","title":"Variability in rainfall at monitoring stations and derivation of a long-term rainfall intensity record in the Grand Canyon Region, Arizona, USA","docAbstract":"In this study, we examine rainfall datasets of varying temporal length, resolution, and spatial distribution to characterize rainfall depth, intensity, and seasonality for monitoring stations along the Colorado River within Marble and Grand Canyons. We identify maximum separation distances between stations at which rainfall measurements might be most useful for inferring rainfall characteristics at other locations. We demonstrate a method for applying relations between daily rainfall depth and intensity, from short-term high-resolution data to lower-resolution longer-term data, to synthesize a long-term record of daily rainfall intensity from 1950–2012. We consider the implications of our spatio-temporal characterization of rainfall for understanding local landscape change in sedimentary deposits and archaeological sites, and for better characterizing past and present rainfall and its potential role in overland flow erosion within the canyons. We find that rainfall measured at stations within the river corridor is spatially correlated at separation distances of tens of kilometers, and is not correlated at the large elevation differences that separate stations along the Colorado River from stations above the canyon rim. These results provide guidance for reasonable separation distances at which rainfall measurements at stations within the Grand Canyon region might be used to infer rainfall at other nearby locations along the river. Like other rugged landscapes, spatial variability between rainfall measured at monitoring stations appears to be influenced by canyon and rim physiography and elevation, with preliminary results suggesting the highest elevation landform in the region, the Kaibab Plateau, may function as an important orographic influence. Stations at specific locations within the canyons and along the river, such as in southern (lower) Marble Canyon and eastern (upper) Grand Canyon, appear to have strong potential to receive high-intensity rainfall that can generate runoff which may erode alluvium. The characterization of past and present rainfall variability in this study will be useful for future studies that evaluate more spatially continuous datasets in order to better understand the rainfall dynamics within this, and potentially other, deep canyons.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20165012","usgsCitation":"Caster, Joshua, and Sankey, J.B., 2016, Variability in rainfall at monitoring stations and derivation of a long-term rainfall intensity record in the Grand Canyon region, Arizona, USA: U.S. Geological Survey Scientific Investigations Report 2016-5012, 38 p., https://dx.doi.org/10.3133/sir20165012.","productDescription":"iv, 38 p.","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-065524","costCenters":[{"id":568,"text":"Southwest Biological Science Center","active":true,"usgs":true}],"links":[{"id":319918,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/sir/2016/5012/cover.jpg"},{"id":319915,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2016/5012/sir20165012.pdf","text":"Report","size":"5.7 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIR 2016-5012 Report"},{"id":319916,"rank":3,"type":{"id":3,"text":"Appendix"},"url":"https://pubs.usgs.gov/sir/2016/5012/sir20165012_appendix4.csv","text":"Appendix 4","size":"400 KB","linkFileType":{"id":7,"text":"csv"},"description":"SIR 2016-5012 Appendix 4"}],"country":"United States","state":"Arizona","otherGeospatial":"Grand Canyon","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -114.0655517578125,\n 35.68407153314097\n ],\n [\n -114.0655517578125,\n 37.02448395075965\n ],\n [\n -111.3629150390625,\n 37.02448395075965\n ],\n [\n -111.3629150390625,\n 35.68407153314097\n ],\n [\n -114.0655517578125,\n 35.68407153314097\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"SBSC Staff, Southwest Biological Science Center
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Technically recoverable undiscovered hydrocarbon resources in continuous accumulations are present in Upper Devonian and Lower Mississippian strata in the Appalachian Basin Petroleum Province. The province includes parts of New York, Pennsylvania, Ohio, Maryland, West Virginia, Virginia, Kentucky, Tennessee, Georgia, and Alabama. The Upper Devonian and Lower Mississippian strata are part of the previously defined Devonian Shale-Middle and Upper Paleozoic Total Petroleum System (TPS) that extends from New York to Tennessee. This publication presents a revision to the extent of the Devonian Shale-Middle and Upper Paleozoic TPS. The most significant modification to the maximum extent of the Devonian Shale-Middle and Upper Paleozoic TPS is to the south and southwest, adding areas in Tennessee, Georgia, Alabama, and Mississippi where Devonian strata, including potential petroleum source rocks, are present in the subsurface up to the outcrop. The Middle to Upper Devonian Chattanooga Shale extends from southeastern Kentucky to Alabama and eastern Mississippi. Production from Devonian shale has been established in the Appalachian fold and thrust belt of northeastern Alabama. Exploratory drilling has encountered Middle to Upper Devonian strata containing organic-rich shale in west-central Alabama. The areas added to the TPS are located in the Valley and Ridge, Interior Low Plateaus, and Appalachian Plateaus physiographic provinces, including the portion of the Appalachian fold and thrust belt buried beneath Cretaceous and younger sediments that were deposited on the U.S. Gulf Coastal Plain.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/ofr20161018","usgsCitation":"Enomoto, C.B., Rouse, W.A., Trippi, M.H., and Higley, D.K., 2016, Revisions to the original extent of the Devonian Shale-Middle and Upper Paleozoic Total Petroleum System: U.S. Geological Survey Open-File Report 2016–1018, 6 p., https://dx.doi.org/10.3133/ofr20161018.","productDescription":"Report: iv, 6 p.; Shapefiles; Metadata Files","onlineOnly":"Y","additionalOnlineFiles":"Y","ipdsId":"IP-068927","costCenters":[{"id":241,"text":"Eastern Energy Resources Science Center","active":true,"usgs":true}],"links":[{"id":319798,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/2016/1018/ofr20161018.pdf","text":"Report","size":"432 KB","linkFileType":{"id":1,"text":"pdf"},"description":"OFR 2016-1018"},{"id":319797,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/2016/1018/coverthb.jpg"},{"id":319922,"rank":3,"type":{"id":23,"text":"Spatial Data"},"url":"https://pubs.usgs.gov/of/2016/1018/ofr20161018_tps506704-metadata.zip","text":"Shapefiles and Metadata Files","size":"1.18 MB","linkFileType":{"id":6,"text":"zip"},"description":"OFR 2016-1018"}],"country":"United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.76220703125,\n 42.779275360241904\n ],\n [\n -78.79394531249999,\n 42.90816007196054\n ],\n [\n -81.5185546875,\n 42.48830197960227\n ],\n [\n -83.232421875,\n 41.623655390686395\n ],\n [\n -84.00146484374999,\n 38.71980474264239\n ],\n [\n -86.17675781249999,\n 36.63316209558658\n ],\n [\n -88.330078125,\n 34.90395296559004\n ],\n [\n -89.67041015625,\n 33.08233672856376\n ],\n [\n -86.396484375,\n 32.76880048488168\n ],\n [\n -81.05712890625,\n 36.58024660149866\n ],\n [\n -77.47558593749999,\n 39.30029918615029\n ],\n [\n -74.35546875,\n 41.1455697310095\n ],\n [\n -73.76220703125,\n 42.779275360241904\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, Eastern Energy Resources Science Center
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http://energy.usgs.gov/
Debris flow magnitudes and frequencies are compared across the Upper Colorado River valley to assess influences on debris flow occurrence and to evaluate valley geometry effects on sediment persistence. Dendrochronology, field mapping, and aerial photographic analysis are used to evaluate whether a 19th century earthen, water-conveyance ditch has altered the regime of debris flow occurrence in the Colorado River headwaters. Identifying any shifts in disturbance processes or changes in magnitudes and frequencies of occurrence is fundamental to establishing the historical range of variability (HRV) at the site. We found no substantial difference in frequency of debris flows cataloged at eleven sites of deposition between the east (8) and west (11) sides of the Colorado River valley over the last century, but four of the five largest debris flows originated on the west side of the valley in association with the earthen ditch, while the fifth is on a steep hillslope of hydrothermally altered rock on the east side. These results suggest that the ditch has altered the regime of debris flow activity in the Colorado River headwaters as compared to HRV by increasing the frequency of debris flows large enough to reach the Colorado River valley. Valley confinement is a dominant control on response to debris flows, influencing volumes of aggradation and persistence of debris flow deposits. Large, frequent debris flows, exceeding HRV, create persistent effects due to valley geometry and geomorphic setting conducive to sediment storage that are easily delineated by valley confinement ratios which are useful to land managers.
","language":"English","publisher":"Springer","doi":"10.1007/s00267-016-0695-1","usgsCitation":"Grimsley, K.J., Rathburn, S.L., Friedman, J.M., and Mangano, J.F., 2016, Debris flow occurrence and sediment persistence, Upper Colorado River Valley, CO: Environmental Management, v. 58, no. 1, p. 76-92, https://doi.org/10.1007/s00267-016-0695-1.","productDescription":"17 p.","startPage":"76","endPage":"92","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-061452","costCenters":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"links":[{"id":327105,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Rocky Mountain National Park, Upper Colorado River Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.87833404541014,\n 40.4090520858275\n ],\n [\n -105.87833404541014,\n 40.50231368920858\n ],\n [\n -105.8144760131836,\n 40.50231368920858\n ],\n [\n -105.8144760131836,\n 40.4090520858275\n ],\n [\n -105.87833404541014,\n 40.4090520858275\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"58","issue":"1","publishingServiceCenter":{"id":2,"text":"Denver PSC"},"noUsgsAuthors":false,"publicationDate":"2016-04-08","publicationStatus":"PW","scienceBaseUri":"57b82db2e4b03fd6b7da3671","contributors":{"authors":[{"text":"Grimsley, Kyle J","contributorId":173887,"corporation":false,"usgs":false,"family":"Grimsley","given":"Kyle","email":"","middleInitial":"J","affiliations":[{"id":6621,"text":"Colorado State University","active":true,"usgs":false}],"preferred":false,"id":646514,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Rathburn, Sara L.","contributorId":140606,"corporation":false,"usgs":false,"family":"Rathburn","given":"Sara","email":"","middleInitial":"L.","affiliations":[{"id":13539,"text":"Department of Geosciences, Colorado State University, Fort Collins, Colorado","active":true,"usgs":false}],"preferred":false,"id":646515,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Friedman, Jonathan M. 0000-0002-1329-0663 friedmanj@usgs.gov","orcid":"https://orcid.org/0000-0002-1329-0663","contributorId":2473,"corporation":false,"usgs":true,"family":"Friedman","given":"Jonathan","email":"friedmanj@usgs.gov","middleInitial":"M.","affiliations":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"preferred":true,"id":646513,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mangano, Joseph F. 0000-0003-4213-8406 jmangano@usgs.gov","orcid":"https://orcid.org/0000-0003-4213-8406","contributorId":4722,"corporation":false,"usgs":true,"family":"Mangano","given":"Joseph","email":"jmangano@usgs.gov","middleInitial":"F.","affiliations":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"preferred":true,"id":646520,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70188535,"text":"70188535 - 2016 - Tomographic Rayleigh-wave group velocities in the Central Valley, California centered on the Sacramento/San Joaquin Delta","interactions":[],"lastModifiedDate":"2017-06-14T15:14:42","indexId":"70188535","displayToPublicDate":"2016-04-08T00:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2314,"text":"Journal of Geophysical Research B: Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Tomographic Rayleigh-wave group velocities in the Central Valley, California centered on the Sacramento/San Joaquin Delta","docAbstract":"If shaking from a local or regional earthquake in the San Francisco Bay region were to rupture levees in the Sacramento/San Joaquin Delta then brackish water from San Francisco Bay would contaminate the water in the Delta: the source of fresh water for about half of California. As a prelude to a full shear-wave velocity model that can be used in computer simulations and further seismic hazard analysis, we report on the use of ambient noise tomography to build a fundamental-mode, Rayleigh-wave group velocity model for the region around the Sacramento/San Joaquin Delta in the western Central Valley, California. Recordings from the vertical component of about 31 stations were processed to compute the spatial distribution of Rayleigh wave group velocities. Complex coherency between pairs of stations were stacked over 8 months to more than a year. Dispersion curves were determined from 4 to about 18 seconds. We calculated average group velocities for each period and inverted for deviations from the average for a matrix of cells that covered the study area. Smoothing using the first difference is applied. Cells of the model were about 5.6 km in either dimension. Checkerboard tests of resolution, which is dependent on station density, suggest that the resolving ability of the array is reasonably good within the middle of the array with resolution between 0.2 and 0.4 degrees. Overall, low velocities in the middle of each image reflect the deeper sedimentary syncline in the Central Valley. In detail, the model shows several centers of low velocity that may be associated with gross geologic features such as faulting along the western margin of the Central Valley, oil and gas reservoirs, and large cross cutting features like the Stockton arch. At shorter periods around 5.5s, the model’s western boundary between low and high velocities closely follows regional fault geometry and the edge of a residual isostatic gravity low. In the eastern part of the valley, the boundaries of the low velocity zone and gravity anomaly are better aligned at longer periods (around 10.5s) suggesting that the eastern edge of the gravity low is associated with deeper structure. There is a strong correspondence between a low in gravity near the Kirby Hills fault and low velocities from the ambient noise tomography. At longer periods, higher velocities creep in from the east and narrow the overall dimension defined by the lower velocities. Overall, there is a strong correspondence between the shape and location of low velocities in the Rayleigh wave velocity images, and geological and geophysical features.","language":"English","publisher":"American Geophysical Union","doi":"10.1002/2015JB012376","usgsCitation":"Fletcher, J.P., Erdem, J., Seats, K., and Lawrence, J., 2016, Tomographic Rayleigh-wave group velocities in the Central Valley, California centered on the Sacramento/San Joaquin Delta: Journal of Geophysical Research B: Solid Earth, v. 121, no. 4, p. 2429-2446, https://doi.org/10.1002/2015JB012376.","productDescription":"18 p. ","startPage":"2429","endPage":"2446","ipdsId":"IP-062590","costCenters":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"links":[{"id":471084,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1002/2015jb012376","text":"Publisher Index Page"},{"id":342506,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Central Valley, 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 -122.7117919921875,\n 39.89709437260048\n ],\n [\n -122.01416015625,\n 38.225235239076824\n ],\n [\n -121.4813232421875,\n 37.63163475580643\n ],\n [\n -121.00341796874999,\n 37.08585785263673\n ],\n [\n -120.67932128906249,\n 36.730079507078415\n ],\n [\n -118.55895996093749,\n 37.53150992479082\n ],\n [\n -118.7017822265625,\n 38.043765107439675\n ],\n [\n -119.08630371093749,\n 38.543869175876154\n ],\n [\n -119.80590820312499,\n 39.317300373271024\n ],\n [\n -120.2838134765625,\n 39.774769485295465\n ],\n [\n -120.948486328125,\n 40.29628651711716\n ],\n [\n -121.31103515625,\n 40.53050177574321\n ],\n [\n -121.97021484374999,\n 40.53050177574321\n ],\n [\n -122.398681640625,\n 40.40094763151963\n ],\n [\n -122.72277832031251,\n 40.225024210604964\n ],\n [\n -122.7117919921875,\n 39.89709437260048\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"121","issue":"4","publishingServiceCenter":{"id":14,"text":"Menlo Park PSC"},"noUsgsAuthors":false,"publicationDate":"2016-04-08","publicationStatus":"PW","scienceBaseUri":"59424b39e4b0764e6c65dc30","contributors":{"authors":[{"text":"Fletcher, Jon Peter B. 0000-0001-8885-6177 jfletcher@usgs.gov","orcid":"https://orcid.org/0000-0001-8885-6177","contributorId":1216,"corporation":false,"usgs":true,"family":"Fletcher","given":"Jon","email":"jfletcher@usgs.gov","middleInitial":"Peter B.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":698169,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Erdem, Jemile 0000-0003-2353-9431 jerdem@usgs.gov","orcid":"https://orcid.org/0000-0003-2353-9431","contributorId":127700,"corporation":false,"usgs":true,"family":"Erdem","given":"Jemile","email":"jerdem@usgs.gov","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":698172,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Seats, Kevin","contributorId":192927,"corporation":false,"usgs":false,"family":"Seats","given":"Kevin","email":"","affiliations":[],"preferred":false,"id":698170,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Lawrence, Jesse","contributorId":192928,"corporation":false,"usgs":false,"family":"Lawrence","given":"Jesse","affiliations":[],"preferred":false,"id":698171,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70170081,"text":"sim3352 - 2016 - Potentiometric surfaces, summer 2013 and winter 2015, and select hydrographs for the Southern High Plains aquifer, Cannon Air Force Base, Curry County, New Mexico","interactions":[],"lastModifiedDate":"2016-04-11T08:44:03","indexId":"sim3352","displayToPublicDate":"2016-04-07T00:00:00","publicationYear":"2016","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":333,"text":"Scientific Investigations Map","code":"SIM","onlineIssn":"2329-132X","printIssn":"2329-1311","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"3352","title":"Potentiometric surfaces, summer 2013 and winter 2015, and select hydrographs for the Southern High Plains aquifer, Cannon Air Force Base, Curry County, New Mexico","docAbstract":"Cannon Air Force Base (Cannon AFB) is located in the High Plains physiographic region of east-central New Mexico, about 5 miles west of Clovis, New Mexico. The area surrounding Cannon AFB is primarily used for agriculture, including irrigated cropland and dairies. The Southern High Plains aquifer is the principal source of water for Cannon AFB, for the nearby town of Clovis, and for local agriculture and dairies. The Southern High Plains aquifer in the vicinity of Cannon AFB consists of three subsurface geological formations: the Chinle Formation of Triassic age, the Ogallala Formation of Tertiary age, and the Blackwater Draw Formation of Quaternary age. The Ogallala Formation is the main water-yielding formation of the Southern High Plains aquifer. Groundwater-supplied, center-pivot irrigation dominates pumping from the Southern High Plains aquifer in the area surrounding Cannon AFB, where the irrigation season typically extends from early March through October. The U.S. Geological Survey has been monitoring groundwater levels in the vicinity of Cannon AFB since 1954 and has developed general potentiometric-surface maps that show groundwater flow from northwest to southeast in the study area. While previous potentiometric-surface maps show the general direction of groundwater flow, a denser well network is needed to show details of groundwater flow at a local scale. Groundwater levels were measured in 93 wells during summer 2013 and 100 wells during winter 2015.
The summer and winter potentiometric-surface maps display the presence of what is interpreted to be a groundwater trough trending from the northwest to the southeast through the study area. This groundwater trough may be the hydraulic expression of a Tertiary-age paleochannel. Groundwater north of the trough flows in a southerly direction into the trough, and groundwater south of the trough flows in an easterly direction into the trough.
During the 18-month period between summer 2013 and winter 2015, changes in groundwater levels ranged from a rise of 10.0 to a decline of 3.8 feet. The regions to the north and south of the groundwater trough contained the majority of the rises in groundwater levels, whereas the regions within the trough contained the majority of the declines in groundwater levels. In contrast, the long-term groundwater-level trend in wells with 20 to 60 years of record is a steady decline in average annual water levels, with declines ranging from 0.41 to 2.81 feet per year. Overall, the northwestern part of the study area exhibits the smallest average annual declines, while the southeastern part of the study area exhibits the largest average annual declines.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sim3352","collaboration":"Prepared in cooperation with the Air Force Civil Engineer Center, San Antonio, Texas","usgsCitation":"Collison, Jake, 2016, Potentiometric surfaces, summer 2013 and winter 2015, and select hydrographs for the Southern High Plains aquifer, Cannon Air Force Base, Curry County, New Mexico: U.S. Geological Survey Scientific Investigations Map 3352, https://dx.doi.org/10.3133/sim3352.","productDescription":"2 Sheets: 22 x 30 inches","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-069490","costCenters":[{"id":472,"text":"New Mexico Water Science Center","active":true,"usgs":true}],"links":[{"id":319842,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sim/3352/sim3352.pdf","text":"Map","size":"3.40 MB","linkFileType":{"id":1,"text":"pdf"},"description":"SIM 3352"},{"id":319796,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/sim/3352/coverthb.jpg"}],"country":"United States","state":"New Mexico","county":"Curry County","otherGeospatial":"Southern High Plains Aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.1997299194336,\n 34.30799463462751\n ],\n [\n -103.20213317871094,\n 34.32472485669068\n ],\n [\n -103.20144653320312,\n 34.349105308603086\n ],\n [\n -103.20144653320312,\n 34.36922801491184\n ],\n [\n -103.20144653320312,\n 34.387079327815805\n ],\n [\n -103.20247650146484,\n 34.415406930259294\n ],\n [\n -103.20281982421875,\n 34.43239888779366\n ],\n [\n -103.20625305175781,\n 34.453350878522286\n ],\n [\n -103.2117462158203,\n 34.45844651413059\n ],\n [\n -103.22410583496094,\n 34.46552326993406\n ],\n [\n -103.23715209960938,\n 34.468353804284924\n ],\n [\n -103.25809478759764,\n 34.469769035464836\n ],\n [\n -103.27869415283203,\n 34.47203335543746\n ],\n [\n -103.29689025878905,\n 34.472599425831355\n ],\n [\n -103.32572937011719,\n 34.47458064197167\n ],\n [\n -103.34152221679688,\n 34.47797690306098\n ],\n [\n -103.36658477783203,\n 34.47882594673332\n ],\n [\n -103.38512420654297,\n 34.477693886583516\n ],\n [\n -103.4036636352539,\n 34.474014585017066\n ],\n [\n -103.40572357177734,\n 34.46920294587255\n ],\n [\n -103.41053009033203,\n 34.45788034775209\n ],\n [\n -103.41053009033203,\n 34.44259240448441\n ],\n [\n -103.41190338134766,\n 34.43466422118617\n ],\n [\n -103.41293334960938,\n 34.41795594404557\n ],\n [\n -103.41361999511719,\n 34.41059191445944\n ],\n [\n -103.41293334960938,\n 34.40237742424137\n ],\n [\n -103.41121673583984,\n 34.39387882699731\n ],\n [\n -103.40744018554688,\n 34.38311269824024\n ],\n [\n -103.4084701538086,\n 34.37206181069581\n ],\n [\n -103.40572357177734,\n 34.361292876752564\n ],\n [\n -103.39508056640625,\n 34.35193978491414\n ],\n [\n -103.3868408203125,\n 34.34627073645813\n ],\n [\n -103.38306427001952,\n 34.336348979311985\n ],\n [\n -103.38272094726561,\n 34.326426048404265\n ],\n [\n -103.37448120117188,\n 34.3207552752374\n ],\n [\n -103.3480453491211,\n 34.31678550602219\n ],\n [\n -103.31817626953125,\n 34.313382697259456\n ],\n [\n -103.2879638671875,\n 34.311397661782244\n ],\n [\n -103.26221466064453,\n 34.30969616544571\n ],\n [\n -103.23646545410156,\n 34.30997975056304\n ],\n [\n -103.21792602539062,\n 34.30714385628804\n ],\n [\n -103.1997299194336,\n 34.30799463462751\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Director, New Mexico Water Science Center
U.S. Geological Survey
5338 Montgomery Blvd. NE, Suite 400
Albuquerque, NM 87109–1311
A large-scale study by the U.S. Geological Survey, in cooperation with the Montana Department of Transportation and the Montana Department of Natural Resources and Conservation, was done to investigate general patterns in peak-flow temporal trends and stationarity through water year 2011 for 24 long-term streamflow-gaging stations (hereinafter referred to as gaging stations) in Montana. Hereinafter, all years refer to water years; a water year is the 12-month period from October 1 through September 30 and is designated by the year in which it ends. The primary focus of the study was to identify general patterns in peak-flow temporal trends and stationarity that are relevant to application of peak-flow frequency analyses within a statewide gaging-station network.
\nTemporal trends were analyzed for two hydrologic variables: annual peak flow and peak-flow timing. Annual peak flow is the maximum instantaneous discharge, in cubic feet per second, recorded each year a gaging station was operated. Peak-flow timing is the day of the annual peak flow (hereinafter referred to as day of peak), recorded each year a gaging station was operated.
\nStudy results provide evidence that annual peak flow for most of the long-term gaging stations can be reasonably considered as stationary for application of peak-flow frequency analyses within a statewide gaging station network. Upward trends in annual peak flow during 1930–76 generally were stronger than downward trends during 1967–2011 for most long-term gaging stations. Statistical distributions of annual peak flow generally were similar among three summary time periods (1930–78, 1979–2011, and the entire period of record). However, for two low-elevation gaging stations in eastern Montana (Poplar River at international boundary [gaging station 06178000] and Powder River at Moorhead, Montana [gaging station 06324500]), substantial downward trends in annual peak flow during 1967–2011 were of similar or stronger magnitude than the upward trends during 1930–76, and the annual-peak-flow medians for 1979–2011 were substantially lower than the medians for the entire period of record.
\nFor peak-flow timing for most long-term gaging stations, differences in trends between 1930–76 and 1967–2011 are variable and not particularly strong. Statistical distributions generally are similar among the summary time periods. However, for two high-elevation gaging stations on a Missouri River headwater tributary (Gallatin River near Gallatin Gateway, Montana [gaging station 06043500] and Gallatin River at Logan, Montana [gaging station 06052500]) and for five high-elevation gaging stations in the Yellowstone River Basin (Yellowstone River at Corwin Springs, Montana [gaging station 06191500], Yellowstone River near Livingston, Montana [gaging station 06192500], Clarks Fork Yellowstone River near Belfry, Montana [gaging station 06207500], Clarks Fork Yellowstone River at Edgar, Montana [gaging station 06208500], and Yellowstone River at Billings, Montana [gaging station 06214500]) downward trends in peak-flow timing during 1967–2011 generally were stronger than upward trends during 1930–1976, and day-of-peak medians for 1979–2011 were considerably less than medians for 1930–78. The downward trends in peak-flow timing for 1967–2011 indicate that the timing of annual peak flows changed from later in the year to earlier in the year. For the seven high-elevation gaging stations, the mean change during 1967–2011 was about 13 days (range of 8 to 22 days).
\nFor most of the high-elevation gaging stations in the Missouri River headwaters, Yellowstone River Basin, and Columbia River Basin, there was general correspondence between trend patterns for annual peak flow and trend patterns for peak-flow timing; that is, during periods when there were upward trends in annual peak flow, there generally also were upward trends in peak-flow timing. Conversely, during periods when there were downward trends in annual peak flow, there generally also were downward trends in peak-flow timing.
\nThe two low-elevation gaging stations in eastern Montana (Poplar River at international boundary [gaging station 06178000] and Powder River at Moorhead, Montana [gaging station 06324500]) had considerable changes in annual-peakflow characteristics after the mid-1970s, which might provide evidence of potential nonstationarity in the peak-flow records. The two low-elevation gaging stations that have potential nonstationarity are located in drainage basins that are strongly affected by agricultural activities that potentially affect the hydrologic regimes. Primary agricultural activities that might alter natural hydrologic conditions include construction of small impoundments (primarily for stock-watering purposes) and irrigation diversions. Temporal variability in these activities might contribute to the potential nonstationarity issues. Changes in climatic characteristics after the mid-1970s also possibly contribute to the potential nonstationarity issues. Lack of considerable indication of potential nonstationarity in annual peak flow for the other long-term gaging stations in this study might indicate that climatic changes have been more pronounced with respect to effects on peak flows in low elevation areas in eastern Montana than in areas represented by the other long-term gaging stations. Another possibility is that climatic changes after the mid-1970s are exacerbated in low-elevation areas where small-impoundment development and potential effects of irrigation diversions might be more extensive.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Montana StreamStats (Scientific Investigations Report 2015-5019)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/sir20155019B","collaboration":"Prepared in cooperation with the Montana Department of Transportation and Montana Department of Natural Resources and Conservation","usgsCitation":"Sando, S.K., McCarthy, P.M., Sando, Roy, and Dutton, D.M., 2016, Temporal trends and stationarity in annual peak flow and peak-flow timing for selected long-term streamflow-gaging stations in or near Montana through water year 2011: U.S. Geological Survey Scientific Investigations Report 2015–5019–B, 48 p., https://dx.doi.org/10.3133/sir20155019B.","productDescription":"vi, 48 p.","numberOfPages":"58","onlineOnly":"Y","additionalOnlineFiles":"N","ipdsId":"IP-060698","costCenters":[{"id":5050,"text":"WY-MT Water Science 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\"}}]}","contact":"Director, Wyoming-Montana Water Science Center
U.S. Geological Survey
3162 Bozeman Ave
Helena, MT 59601
We present a novel formulation of a mark–recapture–resight model that allows estimation of population size, stopover duration, and arrival and departure schedules at migration areas. Estimation is based on encounter histories of uniquely marked individuals and relative counts of marked and unmarked animals. We use a Bayesian analysis of a state–space formulation of the Jolly–Seber mark–recapture model, integrated with a binomial model for counts of unmarked animals, to derive estimates of population size and arrival and departure probabilities. We also provide a novel estimator for stopover duration that is derived from the latent state variable representing the interim between arrival and departure in the state–space model. We conduct a simulation study of field sampling protocols to understand the impact of superpopulation size, proportion marked, and number of animals sampled on bias and precision of estimates. Simulation results indicate that relative bias of estimates of the proportion of the population with marks was low for all sampling scenarios and never exceeded 2%. Our approach does not require enumeration of all unmarked animals detected or direct knowledge of the number of marked animals in the population at the time of the study. This provides flexibility and potential application in a variety of sampling situations (e.g., migratory birds, breeding seabirds, sea turtles, fish, pinnipeds, etc.). Application of the methods is demonstrated with data from a study of migratory sandpipers.
","language":"English","publisher":"The International Biometric Society","doi":"10.1111/biom.12393","usgsCitation":"Lyons, J., Kendall, W., Royle, J., Converse, S., Andres, B.A., and Buchanan, J.B., 2016, Population size and stopover duration estimation using mark–resight data and Bayesian analysis of a superpopulation model: Biometrics, v. 72, no. 1, p. 262-271, https://doi.org/10.1111/biom.12393.","productDescription":"10 p.","startPage":"262","endPage":"271","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-044684","costCenters":[{"id":200,"text":"Coop Res Unit Seattle","active":true,"usgs":true},{"id":50464,"text":"Eastern Ecological Science Center","active":true,"usgs":true}],"links":[{"id":323259,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"72","issue":"1","publishingServiceCenter":{"id":12,"text":"Tacoma PSC"},"noUsgsAuthors":false,"publicationDate":"2015-09-08","publicationStatus":"PW","scienceBaseUri":"57594221e4b04f417c256939","contributors":{"authors":[{"text":"Lyons, James E.","contributorId":35461,"corporation":false,"usgs":true,"family":"Lyons","given":"James E.","affiliations":[],"preferred":false,"id":637860,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kendall, William L. 0000-0003-0084-9891 wkendall@usgs.gov","orcid":"https://orcid.org/0000-0003-0084-9891","contributorId":166709,"corporation":false,"usgs":true,"family":"Kendall","given":"William L.","email":"wkendall@usgs.gov","affiliations":[{"id":200,"text":"Coop Res Unit Seattle","active":true,"usgs":true}],"preferred":false,"id":637450,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Royle, J. Andrew 0000-0003-3135-2167 aroyle@usgs.gov","orcid":"https://orcid.org/0000-0003-3135-2167","contributorId":138865,"corporation":false,"usgs":true,"family":"Royle","given":"J. Andrew","email":"aroyle@usgs.gov","affiliations":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"preferred":false,"id":637451,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Converse, Sarah J.","contributorId":85716,"corporation":false,"usgs":true,"family":"Converse","given":"Sarah J.","affiliations":[],"preferred":false,"id":637861,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Andres, Brad A.","contributorId":68811,"corporation":false,"usgs":true,"family":"Andres","given":"Brad","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":637862,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Buchanan, Joseph B.","contributorId":171532,"corporation":false,"usgs":false,"family":"Buchanan","given":"Joseph","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":637863,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ]}