This report provides results of a rapid assessment of biological carbon stocks and forest biomass carbon sequestration capacity in the conterminous United States. Maps available from the U.S. Department of Agriculture are used to calculate estimates of current organic carbon storage in soils (73 petagrams of carbon, or PgC) and forest biomass (17 PgC). Of these totals, 3.5 PgC of soil organic carbon and 0.8 PgC of forest biomass carbon occur on lands managed by the U.S. Department of the Interior (DOI). Maps of potential vegetation are used to estimate hypothetical forest biomass carbon sequestration capacities that are 3–7 PgC higher than current forest biomass carbon storage in the conterminous United States. Most of the estimated hypothetical additional forest biomass carbon sequestration capacity is accrued in areas currently occupied by agriculture and development. Hypothetical forest biomass carbon sequestration capacities calculated for existing forests and woodlands are within ±1 PgC of estimated current forest biomass carbon storage. Hypothetical forest biomass sequestration capacities on lands managed by the DOI in the conterminous United States are 0–0.4 PgC higher than existing forest biomass carbon storage. Implications for forest and other land management practices are not considered in this report. Uncertainties in the values reported here are large and difficult to quantify, particularly for hypothetical carbon sequestration capacities. Nevertheless, this rapid assessment helps to frame policy and management discussion by providing estimates that can be compared to amounts necessary to reduce predicted future atmospheric carbon dioxide levels.
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C.","contributorId":73708,"corporation":false,"usgs":true,"family":"Reeves","given":"Matt","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":303954,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Rollins, Matthew G.","contributorId":54695,"corporation":false,"usgs":true,"family":"Rollins","given":"Matthew","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":303953,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ,{"id":98029,"text":"ofr20091191 - 2009 - Reconstructing Rodinia by Fitting Neoproterozoic Continental Margins","interactions":[],"lastModifiedDate":"2012-02-10T00:11:55","indexId":"ofr20091191","displayToPublicDate":"2009-12-08T00:00:00","publicationYear":"2009","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":"2009-1191","title":"Reconstructing Rodinia by Fitting Neoproterozoic Continental Margins","docAbstract":"Reconstructions of Phanerozoic tectonic plates can be closely constrained by lithologic correlations across conjugate margins by paleontologic information, by correlation of orogenic belts, by paleomagnetic location of continents, and by ocean floor magmatic stripes. In contrast, Proterozoic reconstructions are hindered by the lack of some of these tools or the lack of their precision. To overcome some of these difficulties, this report focuses on a different method of reconstruction, namely the use of the shape of continents to assemble the supercontinent of Rodinia, much like a jigsaw puzzle. Compared to the vast amount of information available for Phanerozoic systems, such a limited approach for Proterozoic rocks, may seem suspect. However, using the assembly of the southern continents (South America, Africa, India, Arabia, Antarctica, and Australia) as an example, a very tight fit of the continents is apparent and illustrates the power of the jigsaw puzzle method. \r\n\r\nThis report focuses on Neoproterozoic rocks, which are shown on two new detailed geologic maps that constitute the backbone of the study. The report also describes the Neoproterozoic, but younger or older rocks are not discussed or not discussed in detail. \r\n\r\nThe Neoproterozoic continents and continental margins are identified based on the distribution of continental-margin sedimentary and magmatic rocks that define the break-up margins of Rodinia. These Neoproterozoic continental exposures, as well as critical Neo- and Meso-Neoproterozoic tectonic features shown on the two new map compilations, are used to reconstruct the Mesoproterozoic supercontinent of Rodinia. This approach differs from the common approach of using fold belts to define structural features deemed important in the Rodinian reconstruction. Fold belts are difficult to date, and many are significantly younger than the time frame considered here (1,200 to 850 Ma). \r\n\r\nIdentifying Neoproterozoic continental margins, which are primarily extensional in origin, supports recognition of the Neoproterozoic fragmentation pattern of Rodinia and outlines the major continental masses that, prior to the breakup, formed the supercontinent. Using this pattern, Rodinia can be assembled by fitting the pieces together. \r\n\r\nEvidence for Neoproterozoic margins is fragmentary. The most apparent margins are marked by miogeoclinal deposits (passive-margin deposits). The margins can also be outlined by the distribution of continental-margin magmatic-arc rocks, by juvenile ocean-floor rocks, or by the presence of continent-ward extending aulacogens. \r\n\r\nMost of the continental margins described here are Neoproterozoic, and some had an older history suggesting that they were major, long-lived lithospheric flaws. In particular, the western margin of North America appears to have existed for at least 1,470 Ma and to have been reactivated many times in the Neoproterozoic and Phanerozoic. The inheritance of trends from the Mesoproterozoic by the Neoproterozoic is particularly evident along the eastern United States, where a similarity of Mesoproterozoic (Grenville) and Neoproterozoic trends, as well as Paleozoic or Mesozoic trends, is evident. \r\n\r\nThe model of Rodinia presented here is based on both geologic and paleomagnetic information. Geologic evidence is based on the distribution and shape of Neoproterozoic continents and on assembling these continents so as to match the shape, history, and scale of adjoining margins. The proposed model places the Laurasian continents?Baltica, Greenland, and Laurentia?west of the South American continents (Amazonia, Rio de La Plata, and Sa? Francisco). This assembly is indicated by conjugate pairs of Grenville-age rocks on the east side of Laurentia and on the west side of South America. In the model, predominantly late Neoproterozoic magmatic-arc rocks follow the trend of the Grenville rocks. The boundary between South America and Africa is interpreted as the site of a Wilson cycle","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20091191","usgsCitation":"Stewart, J.H., 2009, Reconstructing Rodinia by Fitting Neoproterozoic Continental Margins: U.S. Geological Survey Open-File Report 2009-1191, Report: iv, 94 p.; 3 Plates - Plates 1 & 2: 48 x 36 inches; Plate 3: 22 x 24 inches, https://doi.org/10.3133/ofr20091191.","productDescription":"Report: iv, 94 p.; 3 Plates - Plates 1 & 2: 48 x 36 inches; Plate 3: 22 x 24 inches","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":660,"text":"Western Mineral Resources Science Center","active":false,"usgs":true}],"links":[{"id":125801,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2009_1191.jpg"},{"id":13234,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2009/1191/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ 180,-90 ], [ 180,90 ], [ -180,90 ], [ -180,-90 ], [ 180,-90 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5fe4b07f02db6346dc","contributors":{"authors":[{"text":"Stewart, John H.","contributorId":83086,"corporation":false,"usgs":true,"family":"Stewart","given":"John","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":303942,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":98028,"text":"sim3094 - 2009 - Geologic Map of the southern Inyo Mountains and vicinity, Inyo County, California","interactions":[],"lastModifiedDate":"2014-10-21T09:40:42","indexId":"sim3094","displayToPublicDate":"2009-12-08T00:00:00","publicationYear":"2009","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":"3094","title":"Geologic Map of the southern Inyo Mountains and vicinity, Inyo County, California","docAbstract":"The Inyo Mountains are located in east-central California between Owens Valley on the west and Saline Valley on the east. This map encompasses the southernmost part of the Inyo Mountains and vicinity, which is centered on the high plateau of Conglomerate Mesa and extends from Owens Valley on the west to the Santa Rosa Hills, Lee Flat, and the Nelson Range on the east. The area includes parts of the Cerro Gordo Peak, Nelson Range, Keeler, and Santa Rosa Flat 7.5' quadrangles.
\nSedimentary and volcanic rocks, unconformities, and structural features exposed in the southern Inyo Mountains region provide information critical for reconstructing the complex Paleozoic and Mesozoic tectonic evolution of the southwestern United States. Ordovician to Cretaceous rocks in the map area record a long geologic history during which the continental margin of the western United States gradually changed from a passive tectonic setting in the early and middle Paleozoic to an active tectonic setting in the Jurassic and Cretaceous. A major highlight of the map area is the unusually complete record of late Paleozoic to earliest Mesozoic (Pennsylvanian to Triassic) deformation and sedimentation that marked the transition between the passive and active margin settings. The area also provides an excellent record of Jurassic to Cretaceous deformation and igneous activity that characterized the middle to late Mesozoic active margin. This map provides a detailed depiction of all the Paleozoic and Mesozoic rocks and structural features known in the area. The area also contains important exposures of upper Cenozoic rocks related to the evolution of the Basin and Range province, although detailed mapping of these rocks was beyond the scope of this study.
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The Wilcox Group in southern Arkansas is undifferentiated, while in northeastern Arkansas, the Wilcox Group is subdivided into three units: Flour Island, Fort Pillow Sand, and Old Breastworks Formation. The Wilcox Group crops out in southwestern Arkansas in discontinuous, 1 to 3 mi wide bands. In northeastern Arkansas, the Wilcox Group crops out along a narrow, discontinuous, band along the western edge of Crowleys Ridge.
The Wilcox aquifer provides sources of groundwater in southwestern and northeastern Arkansas. In 2005, reported withdrawals from the Wilcox aquifer in Arkansas totaled 27.0 million gallons per day, most of which came from the northeastern area. Major withdrawals from the aquifer were for public supplies with lesser but locally important withdrawals for commercial, domestic, and industrial uses.
A study was conducted by the U.S. Geological Survey in cooperation with the Arkansas Natural Resources Commission and the Arkansas Geological Survey to determine the water levels associated with the Wilcox aquifer in southwestern and northeastern Arkansas. During February 2009, 58 water-level measurements were made in wells completed in the Wilcox aquifer. The results from this study and previous studies are presented as potentiometric-surface maps, water-level difference maps, and long-term hydrographs.
The direction of groundwater flow in the southwestern area is affected by two potentiometric-surface mounds, one in the north and the other in the southwest, and a cone of depression in the center. The direction of water flowing off of the northern mound of water is generally to the south and east with some to the north. The direction of water flowing off of the southwestern mound is generally to the south and east. The direction of water flowing into the cone of depression is generally from the north, west, and south. The direction of groundwater flow in the northeastern area is generally to the south and southeast, except in the northwestern part of the area where the flow is in a westerly direction towards Paragould. Large groundwater withdrawals have altered the natural direction of flow near centers of pumping at Paragould and West Memphis.
Water-level difference maps for the Wilcox aquifer in Arkansas were constructed using the differences between water-level measurements made during 2003 and 2009 from 52 wells. The difference in water levels between 2003 and 2009 in the southwestern area ranged from -36.4 to 16.0 ft. Water levels rose in the northern parts of the southwestern area, while the water levels in the southern part of the area declined with the exception of one well. The differences in water levels between 2003 and 2009 in the northeastern area ranged from -21.7 to 1.3 ft. Water levels declined throughout the northeastern area with the exception of two wells.
Hydrographs from 42 wells with a minimum of 20 yr of water-level measurements were constructed. Trend lines using linear regression were calculated for the period from 1990 to 2009 to determine the slope in ft/yr for water levels in each well. In the southwestern area, the county mean annual water level rose 0.15 ft/yr in Hot Spring County. County mean annual water levels declined between 0.71 ft/yr and 0.03 ft/yr in Clark, Hempstead, and Nevada counties. In the northeastern area, the county mean annual water level rose 0.46 ft/yr in Greene County. County mean annual water levels declined between 0.03 ft/yr and 2.12 ft/yr in Clay, Craighead, Crittenden, Lee, Mississippi, Poinsett, and St. Francis counties.
","conferenceTitle":"GCAGS 59th Annual Meeting","conferenceDate":"September 27-29, 2009","conferenceLocation":"Shreveport, LA","language":"English","publisher":"The Gulf Coast Association of Geological Societies","usgsCitation":"Pugh, A., and Schrader, T.P., 2009, Hydrogeologic characteristics and water levels of Wilcox aquifer in southwestern and northeastern Arkansas, GCAGS 59th Annual Meeting, Shreveport, LA, September 27-29, 2009, p. 621-636.","productDescription":"16 p.","startPage":"621","endPage":"636","ipdsId":"IP-013697","costCenters":[{"id":129,"text":"Arkansas Water Science Center","active":true,"usgs":true}],"links":[{"id":341830,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arkansas","otherGeospatial":"Wilcox aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n 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L.","email":"apugh@usgs.gov","affiliations":[{"id":129,"text":"Arkansas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":565507,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schrader, Tony P. tpschrad@usgs.gov","contributorId":3027,"corporation":false,"usgs":true,"family":"Schrader","given":"Tony","email":"tpschrad@usgs.gov","middleInitial":"P.","affiliations":[{"id":129,"text":"Arkansas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":696236,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70146259,"text":"70146259 - 2009 - Predicting bed shear stress and its role in sediment dynamics and restoration potential of the Everglades and other vegetated flow systems","interactions":[],"lastModifiedDate":"2018-04-03T12:10:24","indexId":"70146259","displayToPublicDate":"2009-12-01T14:30:00","publicationYear":"2009","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1454,"text":"Ecological Engineering","active":true,"publicationSubtype":{"id":10}},"title":"Predicting bed shear stress and its role in sediment dynamics and restoration potential of the Everglades and other vegetated flow systems","docAbstract":"Entrainment of sediment by flowing water affects topography, habitat suitability, and nutrient cycling in vegetated floodplains and wetlands, impacting ecosystem evolution and the success of restoration projects. Nonetheless, restoration managers lack simple decision-support tools for predicting shear stresses and sediment redistribution potential in different vegetation communities. Using a field-validated numerical model, we developed state-space diagrams that provide these predictions over a range of water-surface slopes, depths, and associated velocities in Everglades ridge and slough vegetation communities. Diminished bed shear stresses and a consequent decrease in bed sediment redistribution are hypothesized causes of a recent reduction in the topographic and vegetation heterogeneity of this ecosystem. Results confirmed the inability of present-day flows to entrain bed sediment. Further, our diagrams showed bed shear stresses to be highly sensitive to emergent vegetation density and water-surface slope but less sensitive to water depth and periphyton or floating vegetation abundance. These findings suggested that instituting a pulsing flow regime could be the most effective means to restore sediment redistribution to the Everglades. However, pulsing flows will not be sufficient to erode sediment from sloughs with abundant spikerush, unless spikerush density first decreases by natural or managed processes. Our methods provide a novel tool for identifying restoration parameters and performance measures in many types of vegetated aquatic environments where sediment erosion and deposition are involved.
","language":"English","publisher":"Elsevier","publisherLocation":"New York, NY","doi":"10.1016/j.ecoleng.2009.09.002","usgsCitation":"Larsen, L., Harvey, J., and Crimaldi, J.P., 2009, Predicting bed shear stress and its role in sediment dynamics and restoration potential of the Everglades and other vegetated flow systems: Ecological Engineering, v. 35, no. 12, p. 1773-1785, https://doi.org/10.1016/j.ecoleng.2009.09.002.","productDescription":"13 p.","startPage":"1773","endPage":"1785","numberOfPages":"13","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-011565","costCenters":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"links":[{"id":299790,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"35","issue":"12","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"55362346e4b0b22a15807ab5","contributors":{"authors":[{"text":"Larsen, Laurel G. lglarsen@usgs.gov","contributorId":1987,"corporation":false,"usgs":true,"family":"Larsen","given":"Laurel G.","email":"lglarsen@usgs.gov","affiliations":[],"preferred":false,"id":544918,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Harvey, Judson 0000-0002-2654-9873 jwharvey@usgs.gov","orcid":"https://orcid.org/0000-0002-2654-9873","contributorId":140228,"corporation":false,"usgs":true,"family":"Harvey","given":"Judson","email":"jwharvey@usgs.gov","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":false,"id":544917,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Crimaldi, John P.","contributorId":58918,"corporation":false,"usgs":true,"family":"Crimaldi","given":"John","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":544919,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":97988,"text":"sir20095223 - 2009 - Estimation of Leakage Potential of Selected Sites in Interstate and Tri-State Canals Using Geostatistical Analysis of Selected Capacitively Coupled Resistivity Profiles, Western Nebraska, 2004","interactions":[],"lastModifiedDate":"2012-03-08T17:16:31","indexId":"sir20095223","displayToPublicDate":"2009-11-12T00:00:00","publicationYear":"2009","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":"2009-5223","title":"Estimation of Leakage Potential of Selected Sites in Interstate and Tri-State Canals Using Geostatistical Analysis of Selected Capacitively Coupled Resistivity Profiles, Western Nebraska, 2004","docAbstract":"With increasing demands for reliable water supplies and availability estimates, groundwater flow models often are developed to enhance understanding of surface-water and groundwater systems. Specific hydraulic variables must be known or calibrated for the groundwater-flow model to accurately simulate current or future conditions. Surface geophysical surveys, along with selected test-hole information, can provide an integrated framework for quantifying hydrogeologic conditions within a defined area. In 2004, the U.S. Geological Survey, in cooperation with the North Platte Natural Resources District, performed a surface geophysical survey using a capacitively coupled resistivity technique to map the lithology within the top 8 meters of the near-surface for 110 kilometers of the Interstate and Tri-State Canals in western Nebraska and eastern Wyoming. Assuming that leakage between the surface-water and groundwater systems is affected primarily by the sediment directly underlying the canal bed, leakage potential was estimated from the simple vertical mean of inverse-model resistivity values for depth levels with geometrically increasing layer thickness with depth which resulted in mean-resistivity values biased towards the surface. This method generally produced reliable results, but an improved analysis method was needed to account for situations where confining units, composed of less permeable material, underlie units with greater permeability.\r\n\r\nIn this report, prepared by the U.S. Geological Survey in cooperation with the North Platte Natural Resources District, the authors use geostatistical analysis to develop the minimum-unadjusted method to compute a relative leakage potential based on the minimum resistivity value in a vertical column of the resistivity model. The minimum-unadjusted method considers the effects of homogeneous confining units. The minimum-adjusted method also is developed to incorporate the effect of local lithologic heterogeneity on water transmission. Seven sites with differing geologic contexts were selected following review of the capacitively coupled resistivity data collected in 2004. A reevaluation of these sites using the mean, minimum-unadjusted, and minimum-adjusted methods was performed to compare the different approaches for estimating leakage potential.\r\n\r\nFive of the seven sites contained underlying confining units, for which the minimum-unadjusted and minimum-adjusted methods accounted for the confining-unit effect. Estimates of overall leakage potential were lower for the minimum-unadjusted and minimum-adjusted methods than those estimated by the mean method. For most sites, the local heterogeneity adjustment procedure of the minimum-adjusted method resulted in slightly larger overall leakage-potential estimates. In contrast to the mean method, the two minimum-based methods allowed the least permeable areas to control the overall vertical permeability of the subsurface. The minimum-adjusted method refined leakage-potential estimation by additionally including local lithologic heterogeneity effects.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095223","collaboration":"Prepared in cooperation with the North Platte Natural Resources District","usgsCitation":"Vrabel, J., Teeple, A., and Kress, W.H., 2009, Estimation of Leakage Potential of Selected Sites in Interstate and Tri-State Canals Using Geostatistical Analysis of Selected Capacitively Coupled Resistivity Profiles, Western Nebraska, 2004: U.S. Geological Survey Scientific Investigations Report 2009-5223, vi, 24 p., https://doi.org/10.3133/sir20095223.","productDescription":"vi, 24 p.","temporalStart":"2004-01-01","temporalEnd":"2004-12-31","costCenters":[{"id":464,"text":"Nebraska Water Science Center","active":true,"usgs":true}],"links":[{"id":126876,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5223.jpg"},{"id":13164,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5223/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0be4b07f02db5fbcc6","contributors":{"authors":[{"text":"Vrabel, Joseph 0000-0002-8773-0764 jvrabel@usgs.gov","orcid":"https://orcid.org/0000-0002-8773-0764","contributorId":1577,"corporation":false,"usgs":true,"family":"Vrabel","given":"Joseph","email":"jvrabel@usgs.gov","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303810,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Teeple, Andrew 0000-0003-1781-8354 apteeple@usgs.gov","orcid":"https://orcid.org/0000-0003-1781-8354","contributorId":1399,"corporation":false,"usgs":true,"family":"Teeple","given":"Andrew ","email":"apteeple@usgs.gov","affiliations":[{"id":583,"text":"Texas Water Science Center","active":true,"usgs":true}],"preferred":false,"id":303809,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kress, Wade H.","contributorId":100475,"corporation":false,"usgs":true,"family":"Kress","given":"Wade","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":303811,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":97964,"text":"sim3065 - 2009 - Geologic map of northeastern Seattle (part of the Seattle North 7.5' x 15' quadrangle), King County, Washington","interactions":[],"lastModifiedDate":"2023-03-23T20:33:31.031542","indexId":"sim3065","displayToPublicDate":"2009-11-03T00:00:00","publicationYear":"2009","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":"3065","title":"Geologic map of northeastern Seattle (part of the Seattle North 7.5' x 15' quadrangle), King County, Washington","docAbstract":"This geologic map, approximately coincident with the east half of the Seattle North 7.5 x 15’ quadrangle (herein, informally called the “Seattle NE map”), covers nearly half of the City of Seattle and reaches from Lake Washington across to the Puget Sound shoreline. Land uses are mainly residential, but extensive commercial districts are located in the Northgate neighborhood, adjacent to the University of Washington, and along the corridors of Aurora Avenue North and Lake City Way. Industrial activity is concentrated along the Lake Washington Ship Canal and around Lake Union. One small piece of land outside of the quadrangle boundaries, at the west edge of the Bellevue North quadrangle, is included on this map for geographic continuity. Conversely, a small area in the northeast corner of the Seattle North quadrangle, on the eastside of Lake Washington, is excluded from this map.
Within the boundaries of the map area are two large urban lakes, including the most heavily visited park in the State of Washington (Green Lake Park); a stream (Thornton Creek) that still hosts anadromous salmon despite having its headwaters in a golfcourse and a shopping center; parts of three cities, with a combined residential population of about 300,000 people; and the region’s premier research institution, the University of Washington. The north boundary of the map is roughly NE 168th Street in the cities of Shoreline and Lake Forest Park, and the south boundary corresponds to Mercer Street in Seattle. The west boundary is 15th Avenue W (and NW), and the east boundary is formed by Lake Washington. Elevations range from sea level to a maximum of 165 m (541 ft), the latter on a broad till-covered knob in the city of Shoreline near the northwest corner of the map. Previous geologic maps of this area include those of Waldron and others (1962), Galster and Laprade (1991), and Yount and others (1993).
Seattle lies within the Puget Lowland, an elongate structural and topographic basin between the Cascade Range and Olympic Mountains. The Seattle area has been glaciated repeatedly during the past two million years by coalescing glaciers that advanced southward from British Columbia. The landscape we see today was molded by cyclic glacial scouring and deposition and later modified by landsliding and stream erosion. The last ice sheet reached the central Puget Sound region about 14,500 years ago, as measured by 14C dating, and it had retreated from this area by 13,650 14C yr B.P. (equivalent calendar years are about 17,600 and 16,600 years ago; Porter and Swanson, 1998). Seattle now sits atop a complex and incomplete succession of interleaved glacial and nonglacial deposits that overlie an irregular bedrock surface. These glacial and nonglacial deposits vary laterally in both texture and thickness, and they contain many local unconformities. In addition, they have been deformed by faults and folds, at least as recently as 1,100 years ago, and this deformation further complicates the geologic record.
The landforms and near-surface deposits that cover much of the Seattle NE map area record a relatively brief, recent interval of the region’s geologic history. The topography is dominated in the north by a broad, fluted, and south-sloping upland plateau, which gives way to a more complex set of elongated hills in the map’s southern half. The valleys of Pipers Creek, Green Lake, and Thornton Creek mark the transition between these two topographic areas. Most of the uplands are mantled by a rolling surface of sand (unit Qva) and till (unit Qvt) deposited during the last occupation of the Puget Lowland by a continental ice sheet. Beneath these ice sheet deposits is a complex succession of older sediments that extends far below sea level across most of the map area. These older sediments are now locally exposed where modern erosion and landslides have sliced through the edge of the upland, and where subglacial processes apparently left these older sediments largely free of overlying sediments. Lack of overlying sediments is particularly evident on the hillslopes above Thornton Creek, adjacent to Lake Washington, and on the flanks of Capitol Hill.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sim3065","collaboration":"Prepared in cooperation with the City of Seattle and the Pacific Northwest Center for Geologic Mapping Studies at the Department of Earth and Space Sciences, University of Washington","usgsCitation":"Booth, D.B., Troost, K.G., and Shimel, S.A., 2009, Geologic map of northeastern Seattle (part of the Seattle North 7.5' x 15' quadrangle), King County, Washington: U.S. Geological Survey Scientific Investigations Map 3065, 1 Plate: 42.00 × 70.32 inches; Metadata; GIS Data Files, https://doi.org/10.3133/sim3065.","productDescription":"1 Plate: 42.00 × 70.32 inches; Metadata; GIS Data Files","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[{"id":647,"text":"Western Earth Surface Processes","active":false,"usgs":true}],"links":[{"id":125877,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sim_3065.jpg"},{"id":13141,"rank":3,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sim/3065/","linkFileType":{"id":5,"text":"html"}},{"id":398784,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_87554.htm"}],"scale":"12000","projection":"Lambert Conformal Conic","country":"United States","state":"Washington","city":"Seattle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.3833,\n 47.625\n ],\n [\n -122.2433,\n 47.625\n ],\n [\n -122.2433,\n 47.75\n ],\n [\n -122.3833,\n 47.75\n ],\n [\n -122.3833,\n 47.625\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a8643","contributors":{"authors":[{"text":"Booth, Derek B.","contributorId":100873,"corporation":false,"usgs":false,"family":"Booth","given":"Derek","email":"","middleInitial":"B.","affiliations":[{"id":6934,"text":"University of Washington","active":true,"usgs":false}],"preferred":false,"id":303732,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Troost, Kathy Goetz","contributorId":35023,"corporation":false,"usgs":true,"family":"Troost","given":"Kathy","email":"","middleInitial":"Goetz","affiliations":[],"preferred":false,"id":303731,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Shimel, Scott A.","contributorId":25252,"corporation":false,"usgs":true,"family":"Shimel","given":"Scott","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":303730,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70043336,"text":"70043336 - 2009 - Comprehensive inter-laboratory calibration of reference materials for δ18O versus VSMOW using various on-line high-temperature conversion techniques","interactions":[],"lastModifiedDate":"2017-06-01T13:34:59","indexId":"70043336","displayToPublicDate":"2009-11-01T00:00:00","publicationYear":"2009","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3233,"text":"Rapid Communications in Mass Spectrometry","active":true,"publicationSubtype":{"id":10}},"displayTitle":"Comprehensive inter-laboratory calibration of reference materials for δ18O versus VSMOW using various on-line high-temperature conversion techniques","title":"Comprehensive inter-laboratory calibration of reference materials for δ18O versus VSMOW using various on-line high-temperature conversion techniques","docAbstract":"Internationally distributed organic and inorganic oxygen isotopic reference materials have been calibrated by six laboratories carrying out more than 5300 measurements using a variety of high-temperature conversion techniques (HTC) in an evaluation sponsored by the International Union of Pure and Applied Chemistry (IUPAC). To aid in the calibration of these reference materials, which span more than 125‰, an artificially enriched reference water (δ18O of +78.91‰) and two barium sulfates (one depleted and one enriched in 18O) were prepared and calibrated relative to VSMOW2 and SLAP reference waters. These materials were used to calibrate the other isotopic reference materials in this study, which yielded:
| Reference material | δ18O and estimated combined uncertainty |
|---|---|
| IAEA-602 benzoic acid | +71.28 ± 0.36‰ |
| USGS35 sodium nitrate | +56.81 ± 0.31‰ |
| IAEA-NO-3 potassium nitrate | +25.32 ± 0.29‰ |
| IAEA-601 benzoic acid | +23.14 ± 0.19‰ |
| IAEA-SO-5 barium sulfate | +12.13 ± 0.33‰ |
| NBS 127 barium sulfate | +8.59 ± 0.26‰ |
| VSMOW2 water | 0‰ |
| IAEA-600 caffeine | −3.48 ± 0.53‰ |
| IAEA-SO-6 barium sulfate | −11.35 ± 0.31‰ |
| USGS34 potassium nitrate | −27.78 ± 0.37‰ |
| SLAP water | −55.5‰ |
The seemingly large estimated combined uncertainties arise from differences in instrumentation and methodology and difficulty in accounting for all measurement bias. They are composed of the 3-fold standard errors directly calculated from the measurements and provision for systematic errors discussed in this paper. A primary conclusion of this study is that nitrate samples analyzed for δ18O should be analyzed with internationally distributed isotopic nitrates, and likewise for sulfates and organics. Authors reporting relative differences of oxygen-isotope ratios (δ18O) of nitrates, sulfates, or organic material should explicitly state in their reports the δ18O values of two or more internationally distributed nitrates (USGS34, IAEA-NO-3, and USGS35), sulfates (IAEA-SO-5, IAEA-SO-6, and NBS 127), or organic material (IAEA-601 benzoic acid, IAEA-602 benzoic acid, and IAEA-600 caffeine), as appropriate to the material being analyzed, had these reference materials been analyzed with unknowns. This procedure ensures that readers will be able to normalize the δ18O values at a later time should it become necessary.
The high-temperature reduction technique for analyzing δ18O and δ2H is not as widely applicable as the well-established combustion technique for carbon and nitrogen stable isotope determination. To obtain the most reliable stable isotope data, materials should be treated in an identical fashion; within the same sequence of analyses, samples should be compared with working reference materials that are as similar in nature and in isotopic composition as feasible.
","language":"English","publisher":"Wiley","doi":"10.1002/rcm.3958","usgsCitation":"Brand, W., Coplen, T.B., Aerts-Bijma, A.T., Bohlke, J., Gehre, M., Geilmann, H., Groning, M., Jansen, H.G., Meijer, H.A., Mroczkowski, S.J., Qi, H., Soergel, K., Stuart-Williams, H., Weise, S.M., and Werner, R.A., 2009, Comprehensive inter-laboratory calibration of reference materials for δ18O versus VSMOW using various on-line high-temperature conversion techniques: Rapid Communications in Mass Spectrometry, v. 23, p. 999-1019, https://doi.org/10.1002/rcm.3958.","productDescription":"21 p.","startPage":"999","endPage":"1019","numberOfPages":"21","ipdsId":"IP-010249","costCenters":[{"id":146,"text":"Branch of Regional Research-Eastern Region","active":false,"usgs":true}],"links":[{"id":269014,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":267270,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1002/rcm.3958"}],"volume":"23","noUsgsAuthors":false,"publicationDate":"2009-03-04","publicationStatus":"PW","scienceBaseUri":"53cd5252e4b0b290850f4756","contributors":{"authors":[{"text":"Brand, Willi A.","contributorId":38866,"corporation":false,"usgs":true,"family":"Brand","given":"Willi A.","affiliations":[],"preferred":false,"id":473416,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Coplen, Tyler B. 0000-0003-4884-6008 tbcoplen@usgs.gov","orcid":"https://orcid.org/0000-0003-4884-6008","contributorId":508,"corporation":false,"usgs":true,"family":"Coplen","given":"Tyler","email":"tbcoplen@usgs.gov","middleInitial":"B.","affiliations":[{"id":37464,"text":"WMA - Laboratory & Analytical Services Division","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true},{"id":27111,"text":"National Water Quality Program","active":true,"usgs":true},{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":true,"id":473413,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Aerts-Bijma, Anita T.","contributorId":85855,"corporation":false,"usgs":true,"family":"Aerts-Bijma","given":"Anita","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":473420,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bohlke, John Karl 0000-0001-5693-6455","orcid":"https://orcid.org/0000-0001-5693-6455","contributorId":84641,"corporation":false,"usgs":true,"family":"Bohlke","given":"John Karl","affiliations":[],"preferred":false,"id":473419,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Gehre, Matthias","contributorId":34004,"corporation":false,"usgs":false,"family":"Gehre","given":"Matthias","email":"","affiliations":[],"preferred":false,"id":473415,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Geilmann, Heike","contributorId":41303,"corporation":false,"usgs":false,"family":"Geilmann","given":"Heike","email":"","affiliations":[{"id":13365,"text":"Max-Planck Institute for Biogeochemistry, Jena, Germany","active":true,"usgs":false}],"preferred":false,"id":473417,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Groning, Manfred","contributorId":47659,"corporation":false,"usgs":true,"family":"Groning","given":"Manfred","affiliations":[],"preferred":false,"id":473418,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Jansen, Henk G.","contributorId":56466,"corporation":false,"usgs":true,"family":"Jansen","given":"Henk","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":696902,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Meijer, Harro A. J.","contributorId":65684,"corporation":false,"usgs":true,"family":"Meijer","given":"Harro","email":"","middleInitial":"A. J.","affiliations":[],"preferred":false,"id":696903,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Mroczkowski, Stanley J. 0000-0001-8026-6025 smroczko@usgs.gov","orcid":"https://orcid.org/0000-0001-8026-6025","contributorId":2628,"corporation":false,"usgs":true,"family":"Mroczkowski","given":"Stanley","email":"smroczko@usgs.gov","middleInitial":"J.","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":true,"id":473414,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Qi, Haiping 0000-0002-8339-744X haipingq@usgs.gov","orcid":"https://orcid.org/0000-0002-8339-744X","contributorId":507,"corporation":false,"usgs":true,"family":"Qi","given":"Haiping","email":"haipingq@usgs.gov","affiliations":[{"id":436,"text":"National Research Program - Eastern Branch","active":true,"usgs":true}],"preferred":true,"id":473412,"contributorType":{"id":1,"text":"Authors"},"rank":11},{"text":"Soergel, Karin","contributorId":45921,"corporation":false,"usgs":true,"family":"Soergel","given":"Karin","email":"","affiliations":[],"preferred":false,"id":696904,"contributorType":{"id":1,"text":"Authors"},"rank":12},{"text":"Stuart-Williams, Hilary","contributorId":24971,"corporation":false,"usgs":true,"family":"Stuart-Williams","given":"Hilary","email":"","affiliations":[],"preferred":false,"id":696905,"contributorType":{"id":1,"text":"Authors"},"rank":13},{"text":"Weise, Stephan M.","contributorId":9487,"corporation":false,"usgs":true,"family":"Weise","given":"Stephan","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":696906,"contributorType":{"id":1,"text":"Authors"},"rank":14},{"text":"Werner, Roland A.","contributorId":187806,"corporation":false,"usgs":false,"family":"Werner","given":"Roland","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":696907,"contributorType":{"id":1,"text":"Authors"},"rank":15}]}} ,{"id":97961,"text":"sir20095213 - 2009 - Comparison of Hydrologic and Water-Quality Characteristics of Two Native Tallgrass Prairie Streams with Agricultural Streams in Missouri and Kansas","interactions":[],"lastModifiedDate":"2012-03-08T17:16:28","indexId":"sir20095213","displayToPublicDate":"2009-10-31T00:00:00","publicationYear":"2009","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":"2009-5213","title":"Comparison of Hydrologic and Water-Quality Characteristics of Two Native Tallgrass Prairie Streams with Agricultural Streams in Missouri and Kansas","docAbstract":"This report presents the results of a study by the U.S. Geological Survey, in cooperation with the Missouri Department of Natural Resources, to analyze and compare hydrologic and water-quality characteristics of tallgrass prairie and agricultural basins located within the historical distribution of tallgrass prairie in Missouri and Kansas. Streamflow and water-quality data from two remnant, tallgrass prairie basins (East Drywood Creek at Prairie State Park, Missouri, and Kings Creek near Manhattan, Kansas) were compared to similar data from agricultural basins in Missouri and Kansas.\r\n\r\nPrairie streams, especially Kings Creek in eastern Kansas, received a higher percentage of base flow and a lower percentage of direct runoff than similar-sized agricultural streams in the region. A larger contribution of direct runoff from the agricultural streams made them much flashier than prairie streams. During 22 years of record, the Kings Creek base-flow component averaged 66 percent of total flow, but base flow was only 16 to 26 percent of flows at agricultural sites of various record periods. The large base-flow component likely is the result of greater infiltration of precipitation in prairie soils and the resulting greater contribution of groundwater to streamflow. The 1- and 3-day annual maximum flows were significantly greater at three agricultural sites than at Kings Creek. The effects of flashier agricultural streams on native aquatic biota are unknown, but may be an important factor in the sustainability of some native aquatic species.\r\n\r\nThere were no significant differences in the distribution of dissolved-oxygen concentrations at prairie and agricultural sites, and some samples from most sites fell below the 5 milligrams per liter Missouri and Kansas standard for the protection of aquatic life. More than 10 percent of samples from the East Drywood Creek prairie stream were less than this standard. These data indicate low dissolved-oxygen concentrations during summer low-flow periods may be a natural phenomenon for small prairie streams in the Osage Plains.\r\n\r\nNutrient concentrations including total nitrogen, ammonia, nitrate, and total phosphorus were significantly less in base-flow and runoff samples from prairie streams than from agricultural streams. The total nitrogen concentration at all sites other than one of two prairie sampling sites were, on occasion, above the U.S. Environmental Protection Agency recommended criterion for total nitrogen for the prevention of nutrient enrichment, and typically were above this recommended criterion in runoff samples at all sites. Nitrate and total phosphorus concentrations in samples from the prairie streams generally were below the U.S. Environmental Protection Agency recommended nutrient criteria in base-flow and runoff samples, whereas samples from agricultural sites generally were below the criteria in base-flow samples and generally above in runoff samples. The lower concentrations of nutrient species in prairie streams is likely because prairies are not fertilized like agricultural basins and prairie basins are able to retain nutrients better than agricultural basins. This retention is enhanced by increased infiltration of precipitation into the prairie soils, decreased surface runoff, and likely less erosion than in agricultural basins.\r\n\r\nStreamflow in the small native prairie streams had more days of zero flow and lower streamflow yields than similar-sized agricultural streams. The prairie streams were at zero flow about 50 percent of the time, and the agricultural streams were at zero flow 25 to 35 percent of the time. Characteristics of the prairie basins that could account for the greater periods of zero flow and lower yields when compared to agricultural streams include greater infiltration, greater interception and evapotranspiration, shallower soils, and possible greater seepage losses in the prairie basins. Another difference between the prairie and agricultural strea","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095213","collaboration":"Prepared in cooperation with the Missouri Department of Natural Resources","usgsCitation":"Heimann, D.C., 2009, Comparison of Hydrologic and Water-Quality Characteristics of Two Native Tallgrass Prairie Streams with Agricultural Streams in Missouri and Kansas: U.S. Geological Survey Scientific Investigations Report 2009-5213, vi, 39 p., https://doi.org/10.3133/sir20095213.","productDescription":"vi, 39 p.","costCenters":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true}],"links":[{"id":125689,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5213.jpg"},{"id":13138,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5213/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -98,37 ], [ -98,41 ], [ -91,41 ], [ -91,37 ], [ -98,37 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b23e4b07f02db6ae3fa","contributors":{"authors":[{"text":"Heimann, David C. 0000-0003-0450-2545 dheimann@usgs.gov","orcid":"https://orcid.org/0000-0003-0450-2545","contributorId":3822,"corporation":false,"usgs":true,"family":"Heimann","given":"David","email":"dheimann@usgs.gov","middleInitial":"C.","affiliations":[{"id":396,"text":"Missouri Water Science Center","active":true,"usgs":true},{"id":36532,"text":"Central Midwest Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303722,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70156883,"text":"70156883 - 2009 - Did intense volcanism trigger the first Late Ordovician icehouse?","interactions":[],"lastModifiedDate":"2015-09-02T10:23:08","indexId":"70156883","displayToPublicDate":"2009-10-29T11:30:00","publicationYear":"2009","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1796,"text":"Geology","active":true,"publicationSubtype":{"id":10}},"title":"Did intense volcanism trigger the first Late Ordovician icehouse?","docAbstract":"Oxygen isotopes measured on Late Ordovician conodonts from Minnesota and Kentucky (United States) were studied to reconstruct the paleotemperature history during late Sandbian to Katian (Mohawkian–Cincinnatian) time. This time interval was characterized by intense volcanism, as shown by the prominent Deicke, Millbrig, and other K-bentonite beds. A prominent carbon isotope excursion (Guttenberg δ13C excursion, GICE) postdates the Millbrig volcanic eruptions, and has been interpreted to reflect a drawdown of atmospheric carbon dioxide and climatic cooling. The oxygen isotope record in conodont apatite contradicts this earlier interpretation. An increase in δ18O of 1.5‰ (Vienna standard mean ocean water) just above the Deicke K-bentonite suggests an abrupt and short-lived cooling that possibly initiated a first short-term glacial episode well before the major Hirnantian glaciation. The decrease in δ18O immediately after the mega-eruptions indicates warming before the GICE, and no cooling is shown in the GICE interval. The coincidence of the Deicke mega-eruption with a cooling event suggests that this major volcanic event had a profound effect on Late Ordovician (late Mohawkian) climate.
","language":"English","publisher":"Geological Society of America","publisherLocation":"Boulder, CO","doi":"10.1130/G30577.1","usgsCitation":"Buggisch, W., Joachimski, M.M., Lehnert, O., Bergstrom, S.M., and Repetski, J.E., 2009, Did intense volcanism trigger the first Late Ordovician icehouse?: Geology, v. 38, no. 4, p. 327-330, https://doi.org/10.1130/G30577.1.","productDescription":"4 p.","startPage":"327","endPage":"330","numberOfPages":"4","onlineOnly":"N","additionalOnlineFiles":"N","ipdsId":"IP-008547","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":307819,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"38","issue":"4","publishingServiceCenter":{"id":9,"text":"Reston PSC"},"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"55e81dafe4b0dacf699e6662","contributors":{"authors":[{"text":"Buggisch, Werner","contributorId":34408,"corporation":false,"usgs":true,"family":"Buggisch","given":"Werner","email":"","affiliations":[],"preferred":false,"id":570969,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Joachimski, Michael M.","contributorId":61316,"corporation":false,"usgs":true,"family":"Joachimski","given":"Michael","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":570970,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lehnert, Oliver","contributorId":36033,"corporation":false,"usgs":true,"family":"Lehnert","given":"Oliver","email":"","affiliations":[],"preferred":false,"id":570971,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bergstrom, S. M.","contributorId":147234,"corporation":false,"usgs":false,"family":"Bergstrom","given":"S.","email":"","middleInitial":"M.","affiliations":[{"id":6714,"text":"Ohio State University, School of Earth Sciences, Columbus, Ohio, USA","active":true,"usgs":false}],"preferred":false,"id":570968,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Repetski, John E. 0000-0002-2298-7120 jrepetski@usgs.gov","orcid":"https://orcid.org/0000-0002-2298-7120","contributorId":2596,"corporation":false,"usgs":true,"family":"Repetski","given":"John","email":"jrepetski@usgs.gov","middleInitial":"E.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":570967,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70154924,"text":"70154924 - 2009 - Influence of Old World bluestem (Bothrichloa ischaemum) monocultures on breeding density of three grassland songbirds in Oklahoma","interactions":[],"lastModifiedDate":"2017-05-31T16:31:21","indexId":"70154924","displayToPublicDate":"2009-10-28T00:00:00","publicationYear":"2009","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"displayTitle":"Influence of Old World bluestem (Bothrichloa ischaemum) monocultures on breeding density of three grassland songbirds in Oklahoma","title":"Influence of Old World bluestem (Bothrichloa ischaemum) monocultures on breeding density of three grassland songbirds in Oklahoma","docAbstract":"Despite persistent and widespread declines of grassland birds in North America, few studies have assessed differences between native grasslands and seeded monocultures as songbird habitat. In the Great Plains, many fields enrolled in the Conservation Reserve Program have been seeded to Old World bluestems (OWB), but there is evidence to suggest that OWB may not provide suitable conditions for several grassland bird species. Our objectives were to investigate the influence of OWB monocultures on vegetation structure, composition, and breeding densities of three common grassland bird species. In 2007, we used distance sampling to survey breeding songbirds in 6 native mixed grass prairie and 6 OWB fields in Garfield, Grant, and Alfalfa counties, Oklahoma. Native mixed grass prairie supported taller and denser vegetation, as well as greater forb cover than OWB fields. Breeding density of Grasshopper Sparrow (Ammodramus savannarum) was higher in OWB monocultures, while density of Dickcissel (Spiza americana) and Eastern Meadowlark (Sturnella magna) was similar among field types.
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Jr. cleslie@usgs.gov","contributorId":145497,"corporation":false,"usgs":true,"family":"Leslie","given":"David M.","suffix":"Jr.","email":"cleslie@usgs.gov","affiliations":[{"id":198,"text":"Coop Res Unit Atlanta","active":true,"usgs":true}],"preferred":false,"id":564367,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70237810,"text":"70237810 - 2009 - Saddle Mountain fault deformation zone, Olympic Peninsula, Washington: Western boundary of the Seattle uplift","interactions":[],"lastModifiedDate":"2022-10-25T12:03:30.46277","indexId":"70237810","displayToPublicDate":"2009-10-25T06:59:57","publicationYear":"2009","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1820,"text":"Geosphere","active":true,"publicationSubtype":{"id":10}},"title":"Saddle Mountain fault deformation zone, Olympic Peninsula, Washington: Western boundary of the Seattle uplift","docAbstract":"The Saddle Mountain fault, first recognized in the early 1970s, is now well mapped in the Hoodsport area, southeastern Olympic Peninsula (northwestern United States), on the basis of light detection and ranging (LIDAR) surveys, aerial photography, and trench excavations. Drowned trees and trench excavations demonstrate that the Saddle Mountain fault produced a MW 6.5–7.0 earthquake 1000–1300 yr ago, likely contemporaneous with the MW 7.5 Seattle fault earthquake 1100 yr ago and with a variety of other fault and landslide activity over a wide region of the Olympic Peninsula and Puget Lowland. This near synchroneity suggests that the Saddle Mountain and Seattle fault may be kinematically linked. Aeromagnetic anomalies and LIDAR topographic scarps define an en echelon sequence of faults along the southeastern Olympic Peninsula of Washington, all active in Holocene time. A detailed analysis of aeromagnetic data suggests that the Saddle Mountain fault extends at least 35 km, from 6 km southwest of Lake Cushman northward to the latitude of the Seattle fault. A magnetic survey over Price Lake using a nonmagnetic canoe illuminated two east-dipping reverse faults with 20 m of vertical offset at 30 m depth associated with 2–4 m of vertical displacement at the topographic surface. Analysis of regional aeromagnetic data indicates that the Seattle fault may extend westward across Hood Canal and into the Olympic Mountains, where it terminates near the northward terminus of the Saddle Mountain fault. The en echelon alignment of the Saddle Mountain and nearby Frigid Creek and Canyon River faults, all active in late Holocene time, reflects a >45-km-long zone of deformation that may accommodate the northward shortening of Puget Lowland crust inboard of the Olympic massif. In this view, the Seattle fault and Saddle Mountain deformation zone form the boundaries of the northward-advancing Seattle uplift.
This report was prepared by the U.S. Geological Survey (USGS) in cooperation with the Pennsylvania Department of Agriculture (PDA) as part of the Pennsylvania Pesticides and Ground Water Strategy (PPGWS). Monitoring data and extensive quality-assurance data on the occurrence of pesticides in ground water during 2003–07 are presented and evaluated; decreases in the land area used for agriculture and corresponding changes in the use of pesticides also are documented. In the Pennsylvania ground waters assessed since 2003, concentrations of pesticides did not exceed any maximum contaminant or health advisory levels established by the U.S. Environmental Protection Agency; PPGWS actions are invoked by the PDA at fractions of these levels and were needed only in areas designated by the PDA for special ground-water protection.
\nPrevious investigations through 1998 of pesticides in Pennsylvania ground water identified land use, as a surrogate for pesticide use, and rock type of the aquifer combined with physiography as key hydrogeologic setting variables for understanding aquifer vulnerability to contamination and the common occurrence of atrazine and metolachlor in ground water. Of 20 major hydrogeologic settings in a framework established in 1999 for pesticide monitoring in Pennsylvania, 9 were identified as priorities for data collection in order to change the monitoring status from \"inadequate\" to \"adequate\" for the PPGWS.
\nAgricultural and forested land-use areas are decreasing because of urban and suburban growth. In the nine hydrogeologic settings evaluated using 1992 and 2001 data, decreases of up to 12 percent for agricultural land and 10 percent for forested land corresponded to increases of up to 11 percent for urban land. Changes in agricultural pesticide use were computed from crop data. For example, from 1996 to 2004–05, atrazine use declined by about 15 percent to 1,314,000 lb/yr (pounds per year) and metolachlor use increased by about 20 percent to 895,000 lb/yr; these compounds are the two most-used agricultural pesticides statewide.
\nIn 2003–07, a baseline assessment of pesticides was conducted in five of nine hydrogeologic settings with inadequate monitoring data—the Blue Ridge crystalline and Triassic Lowland siliciclastic, Eastern Lake surficial, Devonian-Silurian carbonate, Great Valley siliciclastic, and Northeastern Glaciated surficial settings. Between 20 and 30 wells in each setting were monitored. Of the 126 wells sampled, 96 well-water samples were analyzed for at least 52 pesticide compounds at the USGS National Water Quality Laboratory (NWQL) using a method with a minimum reporting level (MRL) at or above 0.002 µg/L (micrograms per liter). Of the 96 well waters analyzed by NWQL, 43 had measureable concentrations of one or more pesticides. Atrazine and (or) deethylatrazine (CIAT), a degradation product of atrazine, were reported at or above the MRL in 39 of the 43 well waters. Neither atrazine nor CIAT were reported at concentrations exceeding 0.10 µg/L; all measured concentrations in these five settings were below PPGWS action levels. Metolachlor was present in 7 of the 43 well waters with measureable concentrations of 1 or more pesticides; however, concentrations were below the MRL. The other 30 samples (10 of 20 wells in the Blue Ridge crystalline and Triassic Lowland siliciclastic setting and all 20 wells in the Eastern Lake surficial setting) were analyzed for at least 19 pesticide compounds at the Pennsylvania Department of Environmental Protection Laboratory (PADEPL); the PADEPL reported no concentrations of pesticides at or above an MRL of 0.10 µg/L.
\nStatistical tests using the NWQL analytical results showed correlations between pesticide occurrence and two indicators of water-quality degradation—the occurrence of total coliform bacteria and nitrate concentration. A 2 × 2 contingency-table test indicated a relation between presence or absence of atrazine or metolachlor and presence or absence of bacteria only for the 10 wells representing the Blue Ridge crystalline and Triassic Lowland siliciclastic setting. Results of Spearman’s rank test showed strong positive correlations in the Devonian-Silurian carbonate setting between 1) the number of pesticides above the MRLs and nitrate concentration, and 2) concentrations of atrazine and nitrate. Atrazine concentration and nitrate concentration also showed a statistically significant positive correlation in the Great Valley siliciclastic setting.
\nAn additional component of baseline monitoring was to evaluate changes in pesticide concentration in water from wells representing hydrogeologic settings most vulnerable to contamination from pesticides. In 2003, 16 wells originally sampled in the 1990s were resampled—4 each in the Appalachian Mountain carbonate, Triassic Lowland siliciclastic, Great Valley carbonate, and Piedmont carbonate settings. Nine of these wells, where pesticide concentrations from 1993 and 2003 were analyzed at the NWQL, were chosen for a paired-sample analysis using concentrations of atrazine and metolachlor. A statistically significant decrease in atrazine concentration was identified using the Wilcoxon signed-rank test (p = 0.004); significant temporal changes in metolachlor concentrations were not observed (p = 0.625).
\nMonitoring in three areas of special ground-water protection, where selected pesticide concentrations in well water were at or above the PPGWS action levels, was done at wells BE 1370 (Berks County, Oley Township), BA 437 (Blair County, North Woodbury Township), and LN 1842 (Lancaster County, Earl Township). Co-occurrence of pesticide-degradation products with parent compounds was documented for the first time in ground-water samples collected from these three wells. Degradation products of atrazine, cyanazine, acetochlor, alachlor, and metolachlor were commonly at larger concentrations than the parent compound in the same water sample. Pesticide occurrence in water from wells neighboring the hot-spot wells was highly variable; however, the same sets of pesticide compounds that were present in wells BA 437, BE 1370, and LN 1842 were present to some degree in water from neighboring wells. To evaluate temporal changes in concentration, nonparametric statistical tests were used to determine overall and seasonal monotonic trends. Concentrations of alachlor, atrazine, metolachlor, and nitrate were examined using the 5-year (2003–07) and the long-term data from wells BA 437 and LN 1842 (1996–2007 and 1995–2007, respectively), and the long-term data for well BE 1370 (1998–2007); results showed either downward trends or no trends. Trends in acetochlor concentrations were tested only at well LN 1842 using the 5-year data; no trends were observed. Homogeneity of trend tests indicated statistically significant downward concentration trends in the long-term data were due to seasonal trends as follows: BA 437—alachlor and atrazine (summer); BE 1370—atrazine and metolachlor (winter) and alachlor (winter and spring); LN 1842—alachlor (summer and fall) and atrazine (spring and fall).
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095139","collaboration":"Prepared in cooperation with the Pennsylvania Department of Agriculture","usgsCitation":"Loper, C.A., Breen, K.J., Zimmerman, T.M., and Clune, J., 2009, Pesticides in ground water in selected agricultural land-use areas and hydrogeologic settings in Pennsylvania, 2003-07: U.S. Geological Survey Scientific Investigations Report 2009-5139, Report: x, 123 p.; Downloads Directory, https://doi.org/10.3133/sir20095139.","productDescription":"Report: x, 123 p.; Downloads Directory","additionalOnlineFiles":"Y","temporalStart":"2003-01-01","temporalEnd":"2007-12-31","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":125608,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5139.jpg"},{"id":287581,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/sir/2009/5139/sir2009-5139.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":13115,"rank":4,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5139/","linkFileType":{"id":5,"text":"html"}},{"id":287582,"rank":2,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/sir/2009/5139/Appendix3.zip","linkFileType":{"id":6,"text":"zip"}}],"country":"United States","state":"Pennsylvania","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -81,38.75 ], [ -81,42.5 ], [ -74,42.5 ], [ -74,38.75 ], [ -81,38.75 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae0e4b07f02db688277","contributors":{"authors":[{"text":"Loper, Connie A.","contributorId":62243,"corporation":false,"usgs":true,"family":"Loper","given":"Connie","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":303659,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Breen, Kevin J. 0000-0002-9447-6469 kjbreen@usgs.gov","orcid":"https://orcid.org/0000-0002-9447-6469","contributorId":219,"corporation":false,"usgs":true,"family":"Breen","given":"Kevin","email":"kjbreen@usgs.gov","middleInitial":"J.","affiliations":[{"id":501,"text":"Office of Science Quality and Integrity","active":true,"usgs":true}],"preferred":true,"id":303656,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Zimmerman, Tammy M. 0000-0003-0842-6981 tmzimmer@usgs.gov","orcid":"https://orcid.org/0000-0003-0842-6981","contributorId":138830,"corporation":false,"usgs":true,"family":"Zimmerman","given":"Tammy","email":"tmzimmer@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":true,"id":303657,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Clune, John W. 0000-0002-3563-1975","orcid":"https://orcid.org/0000-0002-3563-1975","contributorId":56753,"corporation":false,"usgs":true,"family":"Clune","given":"John W.","affiliations":[],"preferred":false,"id":303658,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":97948,"text":"ds470 - 2009 - Terrestrial lidar datasets of New Orleans, Louisiana, levee failures from Hurricane Katrina, August 29, 2005","interactions":[],"lastModifiedDate":"2022-07-20T20:13:42.078059","indexId":"ds470","displayToPublicDate":"2009-10-24T00:00:00","publicationYear":"2009","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":310,"text":"Data Series","code":"DS","onlineIssn":"2327-638X","printIssn":"2327-0271","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"470","title":"Terrestrial lidar datasets of New Orleans, Louisiana, levee failures from Hurricane Katrina, August 29, 2005","docAbstract":"Hurricane Katrina made landfall with the northern Gulf Coast on August 29, 2005, as one of the strongest hurricanes on record. The storm damage incurred in Louisiana included a number of levee failures that led to the inundation of approximately 85 percent of the metropolitan New Orleans area. Whereas extreme levels of storm damage were expected from such an event, the catastrophic failure of the New Orleans levees prompted a quick mobilization of engineering experts to assess why and how particular levees failed. As part of this mobilization, civil engineering members of the United States Geological Survey (USGS) performed terrestrial lidar topographic surveys at major levee failures in the New Orleans area. The focus of the terrestrial lidar effort was to obtain precise measurements of the ground surface to map soil displacements at each levee site, the nonuniformity of levee height freeboard, depth of erosion where scour occurred, and distress in structures at incipient failure. In total, we investigated eight sites in the New Orleans region, including both earth and concrete floodwall levee breaks. The datasets extend from the 17th Street Canal in the Orleans East Bank area to the intersection of the Gulf Intracoastal Waterway (GIWW) with the Mississippi River Gulf Outlet (MRGO) in the New Orleans East area. The lidar scan data consists of electronic files containing millions of surveyed points. These points characterize the topography of each levee’s postfailure or incipient condition and are available for download through online hyperlinks. The data serve as a permanent archive of the catastrophic damage of Hurricane Katrina on the levee systems of New Orleans. Complete details of the data collection, processing, and georeferencing methodologies are provided in this report to assist in the visualization and analysis of the data by future users.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ds470","usgsCitation":"Collins, B., Kayen, R., Minasian, D.L., and Reiss, T., 2009, Terrestrial lidar datasets of New Orleans, Louisiana, levee failures from Hurricane Katrina, August 29, 2005: U.S. Geological Survey Data Series 470, Report: iv, 24 p.; Metadata: Data Folder; DVD-ROM, https://doi.org/10.3133/ds470.","productDescription":"Report: iv, 24 p.; Metadata: Data Folder; DVD-ROM","onlineOnly":"N","additionalOnlineFiles":"Y","temporalStart":"2005-08-29","temporalEnd":"2005-08-29","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true},{"id":645,"text":"Western Coastal and Marine Geology","active":false,"usgs":true}],"links":[{"id":118592,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ds_470.jpg"},{"id":404160,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_87525.htm","linkFileType":{"id":5,"text":"html"}},{"id":13122,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/ds/470/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Louisiana","city":"New Orleans","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -90.125,\n 29.9561\n ],\n [\n -89.92,\n 29.9561\n ],\n [\n -89.92,\n 30.0528\n ],\n [\n -90.125,\n 30.0528\n ],\n [\n -90.125,\n 29.9561\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db6850ab","contributors":{"authors":[{"text":"Collins, Brian D.","contributorId":71641,"corporation":false,"usgs":true,"family":"Collins","given":"Brian D.","affiliations":[],"preferred":false,"id":303679,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kayen, Robert","contributorId":12030,"corporation":false,"usgs":true,"family":"Kayen","given":"Robert","affiliations":[],"preferred":false,"id":303678,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Minasian, Diane L. dminasian@usgs.gov","contributorId":3232,"corporation":false,"usgs":true,"family":"Minasian","given":"Diane","email":"dminasian@usgs.gov","middleInitial":"L.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":303677,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Reiss, Thomas","contributorId":97588,"corporation":false,"usgs":true,"family":"Reiss","given":"Thomas","affiliations":[],"preferred":false,"id":303680,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":97937,"text":"sir20095205 - 2009 - Numerical groundwater-flow model of the Minnelusa and Madison hydrogeologic units in the Rapid City area, South Dakota","interactions":[],"lastModifiedDate":"2017-10-14T12:08:31","indexId":"sir20095205","displayToPublicDate":"2009-10-22T00:00:00","publicationYear":"2009","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":"2009-5205","title":"Numerical groundwater-flow model of the Minnelusa and Madison hydrogeologic units in the Rapid City area, South Dakota","docAbstract":"The city of Rapid City and other water users in the Rapid City area obtain water supplies from the Minnelusa and Madison aquifers, which are contained in the Minnelusa and Madison hydrogeologic units. A numerical groundwater-flow model of the Minnelusa and Madison hydrogeologic units in the Rapid City area was developed to synthesize estimates of water-budget components and hydraulic properties, and to provide a tool to analyze the effect of additional stress on water-level altitudes within the aquifers and on discharge to springs. This report, prepared in cooperation with the city of Rapid City, documents a numerical groundwater-flow model of the Minnelusa and Madison hydrogeologic units for the 1,000-square-mile study area that includes Rapid City and the surrounding area.\r\n\r\nWater-table conditions generally exist in outcrop areas of the Minnelusa and Madison hydrogeologic units, which form generally concentric rings that surround the Precambrian core of the uplifted Black Hills. Confined conditions exist east of the water-table areas in the study area.\r\n\r\nThe Minnelusa hydrogeologic unit is 375 to 800 feet (ft) thick in the study area with the more permeable upper part containing predominantly sandstone and the less permeable lower part containing more shale and limestone than the upper part. Shale units in the lower part generally impede flow between the Minnelusa hydrogeologic unit and the underlying Madison hydrogeologic unit; however, fracturing and weathering may result in hydraulic connections in some areas. The Madison hydrogeologic unit is composed of limestone and dolomite that is about 250 to 610 ft thick in the study area, and the upper part contains substantial secondary permeability from solution openings and fractures. Recharge to the Minnelusa and Madison hydrogeologic units is from streamflow loss where streams cross the outcrop and from infiltration of precipitation on the outcrops (areal recharge).\r\n\r\nMODFLOW-2000, a finite-difference groundwater-flow model, was used to simulate flow in the Minnelusa and Madison hydrogeologic units with five layers. Layer 1 represented the fractured sandstone layers in the upper 250 ft of the Minnelusa hydrogeologic unit, and layer 2 represented the lower part of the Minnelusa hydrogeologic unit. Layer 3 represented the upper 150 ft of the Madison hydrogeologic unit, and layer 4 represented the less permeable lower part. Layer 5 represented an approximation of the underlying Deadwood aquifer to simulate upward flow to the Madison hydrogeologic unit. The finite-difference grid, oriented 23 degrees counterclockwise, included 221 rows and 169 columns with a square cell size of 492.1 ft in the detailed study area that surrounded Rapid City. The northern and southern boundaries for layers 1-4 were represented as no-flow boundaries, and the boundary on the east was represented with head-dependent flow cells. Streamflow recharge was represented with specified-flow cells, and areal recharge to layers 1-4 was represented with a specified-flux boundary. Calibration of the model was accomplished by two simulations: (1) steady-state simulation of average conditions for water years 1988-97 and (2) transient simulations of water years 1988-97 divided into twenty 6-month stress periods.\r\n\r\nFlow-system components represented in the model include recharge, discharge, and hydraulic properties. The steady-state streamflow recharge rate was 42.2 cubic feet per second (ft3/s), and transient streamflow recharge rates ranged from 14.1 to 102.2 ft3/s. The steady-state areal recharge rate was 20.9 ft3/s, and transient areal recharge rates ranged from 1.1 to 98.4 ft3/s. The upward flow rate from the Deadwood aquifer to the Madison hydrogeologic unit was 6.3 ft3/s. Discharge included springflow, water use, flow to overlying units, and regional outflow. The estimated steady-state springflow of 32.8 ft3/s from seven springs was similar to the simulated springflow of 31.6 ft3/s, which included 20.5 ft3","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095205","isbn":"9781411325982","collaboration":"Prepared in cooperation with the city of Rapid City","usgsCitation":"Putnam, L.D., and Long, A.J., 2009, Numerical groundwater-flow model of the Minnelusa and Madison hydrogeologic units in the Rapid City area, South Dakota: U.S. Geological Survey Scientific Investigations Report 2009-5205, viii, 82 p., https://doi.org/10.3133/sir20095205.","productDescription":"viii, 82 p.","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":126875,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5205.jpg"},{"id":13109,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5205/","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"South Dakota","city":"Rapid City","otherGeospatial":"Madison hydrogeologic unit, Minnelusa unit","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.58333333333333,43.833333333333336 ], [ -103.58333333333333,44.416666666666664 ], [ -102.75,44.416666666666664 ], [ -102.75,43.833333333333336 ], [ -103.58333333333333,43.833333333333336 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e48d0e4b07f02db5465e9","contributors":{"authors":[{"text":"Putnam, Larry D. ldputnam@usgs.gov","contributorId":990,"corporation":false,"usgs":true,"family":"Putnam","given":"Larry","email":"ldputnam@usgs.gov","middleInitial":"D.","affiliations":[],"preferred":true,"id":303635,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Long, Andrew J. 0000-0001-7385-8081 ajlong@usgs.gov","orcid":"https://orcid.org/0000-0001-7385-8081","contributorId":989,"corporation":false,"usgs":true,"family":"Long","given":"Andrew","email":"ajlong@usgs.gov","middleInitial":"J.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true},{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303634,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":97920,"text":"pp1727 - 2009 - Late Cenozoic geology and lacustrine history of Searles Valley, Inyo and San Bernardino Counties, California","interactions":[],"lastModifiedDate":"2015-09-14T14:48:21","indexId":"pp1727","displayToPublicDate":"2009-10-17T00:00:00","publicationYear":"2009","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1727","title":"Late Cenozoic geology and lacustrine history of Searles Valley, Inyo and San Bernardino Counties, California","docAbstract":"Searles Valley is an arid, closed basin lying 70 km east of the south end of the Sierra Nevada, California. It is bounded on the east and northeast by the Slate Range, on the west by the Argus Range and Spangler Hills, and on the south by the Lava Mountains; Searles (dry) Lake occupies the north-central part of the valley. During those parts of late Pliocene and Pleistocene time when precipitation and runoff from the east side of the Sierra Nevada into the Owens River were much greater than at present, a chain of as many as five large lakes was created, of which Searles Lake was third. The stratigraphic record left in Searles Valley when that lake expanded, contracted, or desiccated, is fully revealed by cores from beneath the surface of Searles (dry) Lake and partly recorded by sediments cropping out around the edge of the valley. The subsurface record is described elsewhere. This volume includes six geologic maps (scales: 1:50,000 and 1:10,000) and a text that describes the outcrop record, most of which represents sedimentation since 150 ka. Although this outcrop record is discontinuous, it provides evidence indicating the lake's water depths during each expansion, which the subsurface record does not. Maximum-depth lakes rose to the 2,280-ft (695 m) contour, the level of the spillway that led overflowing waters to Panamint Valley; that spillway is about 660 ft (200 m) above the present dry-lake surface. Several rock units of Tertiary and early Quaternary ages crop out in Searles Valley. Siltstone and sandstone of Tertiary age, mostly lacustrine in nature and locally deformed to near-vertical dips, are exposed in the southern part of the valley, as is the younger(?) upper Miocene Bedrock Spring Formation. Unnamed, mostly mafic volcanic rocks of probable Miocene or Pliocene age are exposed along the north and south edges of the basin. Slightly deformed lacustrine sandstones are mapped in the central-southwestern and southern parts of the study area. The Christmas Canyon Formation and deposits mapped as older gravel and older tufa are extensively exposed over much of the basin floor. The older gravel unit and the gravel facies of the Christmas Canyon Formation are boulder alluvial gravels; parts of these units are probably correlative. The lacustrine facies of the Christmas Canyon Formation includes the Lava Creek ash, which is dated at 0.64 Ma; the older tufa deposits may be equivalent in age to those sediments. Most of this study concerns sediments of the newly described Searles Lake Formation, whose deposition spanned the period between about 150 ka and 2 ka. Most of this formation is lacustrine in origin, but it includes interbedded alluvium. To extract as much geologic detail as possible, criteria were developed that permitted (1) intrabasin correlation of some thin outcrop units representative of only a few thousand years (or less), (2) identification of unconformities produced by subaerial erosion, (3) identification of unconformities produced by sublacustrine erosion, and (4) correlation of outcrop units with subsurface units. The Searles Lake Formation is divided into seven main units, many of which are subdivided on the five larger scale geologic maps. Units A (oldest), B, C, and D are dominantly lacustrine in origin. The Pleistocene-Holocene boundary is placed at the top of unit C. In areas that were a kilometer or more from shore at the time of deposition, deposits of units A,B, and C consist of fine, highly calcareous sand, silt, or clay; nearer to shore they consist of well-sorted coarse sand and gravel. Unit A has been locally subdivided into as many as four subunits, unit B into six subunits, and unit C into six subunits. The finer facies of units A, B, and C contain such high percentages of Caco3 that they are best described as marl. Sediments of unit C, and to a lesser extent those of unit B, are laminated with light- to white-colored layers of aragonite, calcite, or dolomite(?) that may repre
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/pp1727","usgsCitation":"Smith, G.I., 2009, Late Cenozoic geology and lacustrine history of Searles Valley, Inyo and San Bernardino Counties, California: U.S. Geological Survey Professional Paper 1727, Report: viii, 117 p.; 4 Plates: 33 x 40 inches or smaller; Readme; Metadata; Database; Shapefiles, https://doi.org/10.3133/pp1727.","productDescription":"Report: viii, 117 p.; 4 Plates: 33 x 40 inches or smaller; Readme; Metadata; Database; Shapefiles","numberOfPages":"128","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":227,"text":"Earth Surface Dynamics Program","active":true,"usgs":true}],"links":[{"id":125530,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/pp_1727.jpg"},{"id":266880,"type":{"id":16,"text":"Metadata"},"url":"https://pubs.usgs.gov/pp/1727/SearlesValley_metadata.txt"},{"id":266879,"type":{"id":20,"text":"Read Me"},"url":"https://pubs.usgs.gov/pp/1727/1_readme.txt"},{"id":266881,"type":{"id":9,"text":"Database"},"url":"https://pubs.usgs.gov/pp/1727/pp1727searles_valley_db.zip"},{"id":266882,"type":{"id":7,"text":"Companion Files"},"url":"https://pubs.usgs.gov/pp/1727/pp1727searles_valley_shape.zip"},{"id":13092,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/1727/","linkFileType":{"id":5,"text":"html"}},{"id":266875,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1727/pp1727_plate1.pdf"},{"id":266876,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1727/pp1727_plate2.pdf"},{"id":266877,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1727/pp1727_plate3.pdf"},{"id":266874,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1727/pp1727_text.pdf"},{"id":266878,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1727/pp1727_plate4.pdf"}],"projection":"Polyconic","country":"United States","state":"California","county":"Inyo County, San Bernadino County","otherGeospatial":"Searless Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -117.5,35.5 ], [ -117.5,36 ], [ -117,36 ], [ -117,35.5 ], [ -117.5,35.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a8d40","contributors":{"authors":[{"text":"Smith, George I.","contributorId":92637,"corporation":false,"usgs":true,"family":"Smith","given":"George","email":"","middleInitial":"I.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":303587,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":97921,"text":"ofr20091235 - 2009 - A New Occurrence Model for National Assessment of Undiscovered Volcanogenic Massive Sulfide Deposits","interactions":[],"lastModifiedDate":"2018-11-19T10:00:27","indexId":"ofr20091235","displayToPublicDate":"2009-10-17T00:00:00","publicationYear":"2009","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":"2009-1235","title":"A New Occurrence Model for National Assessment of Undiscovered Volcanogenic Massive Sulfide Deposits","docAbstract":"Volcanogenic massive sulfide (VMS) deposits are very significant current and historical resources of Cu-Pb-Zn-Au-Ag, are active exploration targets in several areas of the United States and potentially have significant environmental effects. This new USGS VMS deposit model provides a comprehensive review of deposit occurrence and ore genesis, and fully integrates recent advances in the understanding of active seafloor VMS-forming environments, and integrates consideration of geoenvironmental consequences of mining VMS deposits.\r\n\r\nBecause VMS deposits exhibit a broad range of geological and geochemical characteristics, a suitable classification system is required to incorporate these variations into the mineral deposit model. We classify VMS deposits based on compositional variations in volcanic and sedimentary host rocks. The advantage of the classification method is that it provides a closer linkage between tectonic setting and lithostratigraphic assemblages, and an increased predictive capability during field-based studies.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20091235","usgsCitation":"Shanks, W.P., Dusel-Bacon, C., Koski, R., Morgan, L.A., Mosier, D., Piatak, N., Ridley, I., Seal, R., Schulz, K.J., Slack, J.F., and Thurston, R., 2009, A New Occurrence Model for National Assessment of Undiscovered Volcanogenic Massive Sulfide Deposits: U.S. Geological Survey Open-File Report 2009-1235, iv, 27 p., https://doi.org/10.3133/ofr20091235.","productDescription":"iv, 27 p.","onlineOnly":"Y","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":125509,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2009_1235.jpg"},{"id":13093,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2009/1235/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd495ee4b0b290850ef1b7","contributors":{"authors":[{"text":"Shanks, W.C. Pat III","contributorId":93949,"corporation":false,"usgs":true,"family":"Shanks","given":"W.C.","suffix":"III","email":"","middleInitial":"Pat","affiliations":[],"preferred":false,"id":303598,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dusel-Bacon, Cynthia 0000-0001-8481-739X cdusel@usgs.gov","orcid":"https://orcid.org/0000-0001-8481-739X","contributorId":2797,"corporation":false,"usgs":true,"family":"Dusel-Bacon","given":"Cynthia","email":"cdusel@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":303591,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Koski, Randolph","contributorId":88049,"corporation":false,"usgs":true,"family":"Koski","given":"Randolph","affiliations":[],"preferred":false,"id":303597,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Morgan, Lisa A.","contributorId":66300,"corporation":false,"usgs":true,"family":"Morgan","given":"Lisa","email":"","middleInitial":"A.","affiliations":[{"id":481,"text":"Northern Rocky Mountain Science Center","active":true,"usgs":true}],"preferred":false,"id":303595,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Mosier, Dan","contributorId":36246,"corporation":false,"usgs":true,"family":"Mosier","given":"Dan","affiliations":[],"preferred":false,"id":303594,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Piatak, Nadine M.","contributorId":23621,"corporation":false,"usgs":true,"family":"Piatak","given":"Nadine M.","affiliations":[],"preferred":false,"id":303593,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Ridley, Ian","contributorId":23244,"corporation":false,"usgs":true,"family":"Ridley","given":"Ian","email":"","affiliations":[],"preferred":false,"id":303592,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Seal, Robert R. II 0000-0003-0901-2529 rseal@usgs.gov","orcid":"https://orcid.org/0000-0003-0901-2529","contributorId":397,"corporation":false,"usgs":true,"family":"Seal","given":"Robert R.","suffix":"II","email":"rseal@usgs.gov","affiliations":[],"preferred":false,"id":303588,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Schulz, Klaus J. 0000-0003-2967-4765 kschulz@usgs.gov","orcid":"https://orcid.org/0000-0003-2967-4765","contributorId":2438,"corporation":false,"usgs":true,"family":"Schulz","given":"Klaus","email":"kschulz@usgs.gov","middleInitial":"J.","affiliations":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":303590,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Slack, John F. 0000-0001-6600-3130 jfslack@usgs.gov","orcid":"https://orcid.org/0000-0001-6600-3130","contributorId":1032,"corporation":false,"usgs":true,"family":"Slack","given":"John","email":"jfslack@usgs.gov","middleInitial":"F.","affiliations":[{"id":387,"text":"Mineral Resources Program","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":303589,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Thurston, Roland","contributorId":69261,"corporation":false,"usgs":true,"family":"Thurston","given":"Roland","affiliations":[],"preferred":false,"id":303596,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":97904,"text":"sir20095068 - 2009 - Characteristics of the April 2007 Flood at 10 Streamflow-Gaging Stations in Massachusetts","interactions":[],"lastModifiedDate":"2012-03-08T17:16:27","indexId":"sir20095068","displayToPublicDate":"2009-10-06T00:00:00","publicationYear":"2009","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":"2009-5068","title":"Characteristics of the April 2007 Flood at 10 Streamflow-Gaging Stations in Massachusetts","docAbstract":"A large 'nor'easter' storm on April 15-18, 2007, brought heavy rains to the southern New England region that, coupled with normal seasonal high flows and associated wet soil-moisture conditions, caused extensive flooding in many parts of Massachusetts and neighboring states. To characterize the magnitude of the April 2007 flood, a peak-flow frequency analysis was undertaken at 10 selected streamflow-gaging stations in Massachusetts to determine the magnitude of flood flows at 5-, 10-, 25-, 50-, 100-, 200-, and 500-year return intervals. The magnitude of flood flows at various return intervals were determined from the logarithms of the annual peaks fit to a Pearson Type III probability distribution. Analysis included augmenting the station record with longer-term records from one or more nearby stations to provide a common period of comparison that includes notable floods in 1936, 1938, and 1955.\r\n\r\nThe April 2007 peak flow was among the highest recorded or estimated since 1936, often ranking between the 3d and 5th highest peak for that period. In general, the peak-flow frequency analysis indicates the April 2007 peak flow has an estimated return interval between 25 and 50 years; at stations in the northeastern and central areas of the state, the storm was less severe resulting in flows with return intervals of about 5 and 10 years, respectively. At Merrimack River at Lowell, the April 2007 peak flow approached a 100-year return interval that was computed from post-flood control records and the 1936 and 1938 peak flows adjusted for flood control.\r\n\r\nIn general, the magnitude of flood flow for a given return interval computed from the streamflow-gaging station period-of-record was greater than those used to calculate flood profiles in various community flood-insurance studies. In addition, the magnitude of the updated flood flow and current (2008) stage-discharge relation at a given streamflow-gaging station often produced a flood stage that was considerably different than the flood stage indicated in the flood-insurance study flood profile at that station.\r\n\r\nEquations for estimating the flow magnitudes for 5-, 10-, 25-, 50-, 100-, 200-, and 500-year floods were developed from the relation of the magnitude of flood flows to drainage area calculated from the six streamflow-gaging stations with the longest unaltered record. These equations produced a more conservative estimate of flood flows (higher discharges) than the existing regional equations for estimating flood flows at ungaged rivers in Massachusetts. Large differences in the magnitude of flood flows for various return intervals determined in this study compared to results from existing regional equations and flood insurance studies indicate a need for updating regional analyses and equations for estimating the expected magnitude of flood flows in Massachusetts.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095068","isbn":"9781411325005","collaboration":"Prepared in cooperation with the U.S. Department of Homeland Security Federal Emergency Management Agency","usgsCitation":"Zarriello, P.J., and Carlson, C.S., 2009, Characteristics of the April 2007 Flood at 10 Streamflow-Gaging Stations in Massachusetts: U.S. Geological Survey Scientific Investigations Report 2009-5068, viii, 68 p., https://doi.org/10.3133/sir20095068.","productDescription":"viii, 68 p.","temporalStart":"2007-04-15","temporalEnd":"2007-04-18","costCenters":[{"id":377,"text":"Massachusetts-Rhode Island Water Science Center","active":false,"usgs":true}],"links":[{"id":126867,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5068.jpg"},{"id":13077,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5068/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -73.75,41.25 ], [ -73.75,43.5 ], [ -69.75,43.5 ], [ -69.75,41.25 ], [ -73.75,41.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e2e4b07f02db5e4eae","contributors":{"authors":[{"text":"Zarriello, Phillip J. 0000-0001-9598-9904 pzarriel@usgs.gov","orcid":"https://orcid.org/0000-0001-9598-9904","contributorId":1868,"corporation":false,"usgs":true,"family":"Zarriello","given":"Phillip","email":"pzarriel@usgs.gov","middleInitial":"J.","affiliations":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303544,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carlson, Carl S. 0000-0001-7142-3519 cscarlso@usgs.gov","orcid":"https://orcid.org/0000-0001-7142-3519","contributorId":1694,"corporation":false,"usgs":true,"family":"Carlson","given":"Carl","email":"cscarlso@usgs.gov","middleInitial":"S.","affiliations":[{"id":376,"text":"Massachusetts Water Science Center","active":true,"usgs":true},{"id":466,"text":"New England Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303543,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":97890,"text":"sir20095208 - 2009 - Shallow Groundwater Movement in the Skagit River Delta Area, Skagit County, Washington","interactions":[],"lastModifiedDate":"2012-03-08T17:16:31","indexId":"sir20095208","displayToPublicDate":"2009-10-03T00:00:00","publicationYear":"2009","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":"2009-5208","title":"Shallow Groundwater Movement in the Skagit River Delta Area, Skagit County, Washington","docAbstract":"Shallow groundwater movement in an area between the lower Skagit River and Puget Sound was characterized by the U.S. Geological Survey to assist Skagit County and the Washington State Department of Ecology with the identification of areas where water withdrawals from existing and new wells could adversely affect streamflow in the Skagit River. The shallow groundwater system consists of alluvial, lahar runout, and recessional outwash deposits composed of sand, gravel, and cobbles, with minor lenses of silt and clay. Upland areas are underlain by glacial till and outwash deposits that show evidence of terrestrial and shallow marine depositional environments. Bedrock exposures are limited to a few upland outcrops in the southwestern part of the study area, and consist of metamorphic, sedimentary, and igneous rocks.\r\n\r\nWater levels were measured in 47 wells on a quarterly basis (August 2007, November 2007, February 2008, and May 2008). Measurements from 34 wells completed in the shallow groundwater system were used to construct groundwater-level and flow-direction maps and perform a linear-regression analysis to estimate the overall, time averaged shallow groundwater-flow direction and gradient. Groundwater flow in the shallow groundwater system generally moves in a southwestward direction away from the Skagit River and toward the Swinomish Channel and Skagit Bay. Local groundwater flow towards the river was inferred during February 2008 in areas west and southwest of Mount Vernon. Water-level altitudes varied seasonally, however, and generally ranged from less than 3 feet (August 2007) in the west to about 15 feet (May 2008) in the east. The time-averaged, shallow groundwater-flow direction derived from regression analysis, 8.5 deg south of west, was similar to flow directions depicted on the quarterly water-level maps.\r\n\r\nSeasonal changes in groundwater levels in most wells in the Skagit River Delta follow a typical pattern for shallow wells in western Washington. Water levels rise from October through March, when precipitation is high, and decline from April through September, when precipitation is lower. Groundwater levels in wells along the eastern margin of the study area also are likely influenced by stage on the Skagit River. Water levels in these wells remained elevated through April, and did not seem to begin to decline until the end of May in response to declining river stage. Groundwater levels in a well equipped with a continuous water-level recorder exhibited periodic fluctuations that are characteristic of ocean tides. This well is less than 1 mile east of the tidally influenced Swinomish Channel, and exhibited water-level fluctuations that correspond closely to predicted tidal extremes obtained from a tide gage near La Conner, Washington.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095208","collaboration":"Prepared in cooperation with the Skagit County Public Works Department, Washington State Department of Ecology, and Skagit County Public Utility District No. 1","usgsCitation":"Savoca, M.E., Johnson, K.H., and Fasser, E.T., 2009, Shallow Groundwater Movement in the Skagit River Delta Area, Skagit County, Washington: U.S. Geological Survey Scientific Investigations Report 2009-5208, iv, 23 p., https://doi.org/10.3133/sir20095208.","productDescription":"iv, 23 p.","temporalStart":"2007-08-01","temporalEnd":"2008-05-31","costCenters":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"links":[{"id":125688,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5208.jpg"},{"id":13064,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5208/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122.53333333333333,48.35 ], [ -122.53333333333333,48.483333333333334 ], [ -122.33333333333333,48.483333333333334 ], [ -122.33333333333333,48.35 ], [ -122.53333333333333,48.35 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fae4b07f02db5f42a2","contributors":{"authors":[{"text":"Savoca, Mark E. mesavoca@usgs.gov","contributorId":1961,"corporation":false,"usgs":true,"family":"Savoca","given":"Mark","email":"mesavoca@usgs.gov","middleInitial":"E.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303495,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Johnson, Kenneth H. johnson@usgs.gov","contributorId":3103,"corporation":false,"usgs":true,"family":"Johnson","given":"Kenneth","email":"johnson@usgs.gov","middleInitial":"H.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303496,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Fasser, Elisabeth T. 0000-0002-3945-6633 efasser@usgs.gov","orcid":"https://orcid.org/0000-0002-3945-6633","contributorId":3973,"corporation":false,"usgs":true,"family":"Fasser","given":"Elisabeth","email":"efasser@usgs.gov","middleInitial":"T.","affiliations":[{"id":622,"text":"Washington Water Science Center","active":true,"usgs":true}],"preferred":true,"id":303497,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":97899,"text":"sim2940 - 2009 - Geologic Map of the North Cascade Range, Washington","interactions":[],"lastModifiedDate":"2012-02-10T00:11:53","indexId":"sim2940","displayToPublicDate":"2009-10-03T00:00:00","publicationYear":"2009","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":"2940","title":"Geologic Map of the North Cascade Range, Washington","docAbstract":"The North Cascade Range, commonly referred to as the North Cascades, is the northern part of the Cascade Range that stretches from northern California into British Columbia, where it merges with the Coast Mountains of British Columbia at the Fraser River. The North Cascades are generally characterized by exposure of plutonic and metamorphic rocks in contrast to the volcanic terrain to the south. The rocks of the North Cascades are more resistant to erosion, display greater relief, and show evidence of more pronounced uplift and recent glaciation. Although the total length of the North Cascade Range, extending north from Snoqualmie Pass in Washington, is about 200 mi (320 km), this compilation map at 1:200,000 scale covers only that part (~150 mi) in the United States. The compilation map is derived mostly from eight 1:100,000-scale quadrangle maps that include all of the North Cascade Range in Washington and a bit of the mostly volcanic part of the Cascade Range to the south (fig. 1, sheet 2). Overall, the area represented by this compilation is about 12,740 mi2 (33,000 km2). \r\n\r\nThe superb alpine scenery of the North Cascade Range and its proximity to major population centers has led to designation of much of the area for recreational use or wilderness preservation. A major part of the map area is in North Cascade National Park. Other restricted use areas are the Alpine Lakes, Boulder River, Clearwater, Glacier Peak, Henry M. Jackson, Lake Chelan-Sawtooth, Mount Baker, Noisy-Diobsud, Norse Peak, and Pasayten Wildernesses and the Mount Baker, Lake Chelan, and Ross Lake National Recreation Areas. The valleys traversed by Washington State Highway 20 east of Ross Lake are preserved as North Cascades Scenic Highway. \r\n\r\nThe map area is traversed by three major highways: U.S. Interstate 90, crossing Snoqualmie Pass; Washington State Highway 2, crossing Stevens Pass; and Washington State Highway 20, crossing Washington Pass. Major secondary roads, as well as a network of U.S. Forest Service roads and a few private roads mainly used for logging, are restricted mostly to the flanks of the range. Although much of the mountainous core is inaccessible to automobiles, numerous trails serve the foot or horse traveler.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/sim2940","collaboration":"Prepared in cooperation with Washington State Division of Geology and Earth Resources, U.S. National Park Service, and U.S. Forest Service","usgsCitation":"Haugerud, R.A., and Tabor, R.W., 2009, Geologic Map of the North Cascade Range, Washington: U.S. Geological Survey Scientific Investigations Map 2940, 2 Sheets: Sheet 1 - 35.5 x 52.5 inches, Sheet 2 - 45.5 x 40 inches; 2 Pamphlets: 32 p. & 26 p.; Photo Presentation, https://doi.org/10.3133/sim2940.","productDescription":"2 Sheets: Sheet 1 - 35.5 x 52.5 inches, Sheet 2 - 45.5 x 40 inches; 2 Pamphlets: 32 p. & 26 p.; Photo Presentation","onlineOnly":"Y","additionalOnlineFiles":"Y","costCenters":[{"id":671,"text":"Western Region Geology and Geophysics Science Center","active":false,"usgs":true}],"links":[{"id":246701,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_87446.htm","linkFileType":{"id":5,"text":"html"},"description":"87446"},{"id":125533,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sim_2940.jpg"},{"id":13073,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sim/2940/","linkFileType":{"id":5,"text":"html"}}],"scale":"200000","projection":"Universal Transverse Mercator","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122,47 ], [ -122,49 ], [ -120,49 ], [ -120,47 ], [ -122,47 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db64969f","contributors":{"authors":[{"text":"Haugerud, Ralph A. 0000-0001-7302-4351 rhaugerud@usgs.gov","orcid":"https://orcid.org/0000-0001-7302-4351","contributorId":2691,"corporation":false,"usgs":true,"family":"Haugerud","given":"Ralph","email":"rhaugerud@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":303529,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tabor, Rowland W. rtabor@usgs.gov","contributorId":3816,"corporation":false,"usgs":true,"family":"Tabor","given":"Rowland","email":"rtabor@usgs.gov","middleInitial":"W.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":303530,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":97897,"text":"ofr20081369 - 2009 - Thatcher Bay, Washington, Nearshore Restoration Assessment","interactions":[],"lastModifiedDate":"2012-02-10T00:11:49","indexId":"ofr20081369","displayToPublicDate":"2009-10-03T00:00:00","publicationYear":"2009","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":"2008-1369","title":"Thatcher Bay, Washington, Nearshore Restoration Assessment","docAbstract":"The San Juan Archipelago, located at the confluence of the Puget Sound, the Straits of Juan de Fuca in Washington State, and the Straits of Georgia, British Columbia, Canada, provides essential nearshore habitat for diverse salmonid, forage fish, and bird populations. With 408 miles of coastline, the San Juan Islands provide a significant portion of the available nearshore habitat for the greater Puget Sound and are an essential part of the regional efforts to restore Puget Sound (Puget Sound Shared Strategy 2005). The nearshore areas of the San Juan Islands provide a critical link between the terrestrial and marine environments. For this reason the focus on restoration and conservation of nearshore habitat in the San Juan Islands is of paramount importance.\r\n\r\nWood-waste was a common by-product of historical lumber-milling operations. To date, relatively little attention has been given to the impact of historical lumber-milling operations in the San Juan Archipelago. Thatcher Bay, on Blakely Island, located near the east edge of the archipelago, is presented here as a case study on the restoration potential for a wood-waste contaminated nearshore area. Case study components include (1) a brief discussion of the history of milling operations. (2) an estimate of the location and amount of the current distribution of wood-waste at the site, (3) a preliminary examination of the impacts of wood-waste on benthic flora and fauna at the site, and (4) the presentation of several restoration alternatives for the site.\r\n\r\nThe history of milling activity in Thatcher Bay began in 1879 with the construction of a mill in the southeastern part of the bay. Milling activity continued for more than 60 years, until the mill closed in 1942. Currently, the primary evidence of the historical milling operations is the presence of approximately 5,000 yd3 of wood-waste contaminated sediments. The distribution and thickness of residual wood-waste at the site was determined by using sediment coring and GIS-based interpolation techniques. Additionally, pilot studies were conducted to characterize in place sediment redox, organic composition, and sulfide impacts to nearshore flora and fauna.\r\n\r\nWe found that the presence of wood-waste in Thatcher Bay may alter the quality of the benthic habitat by contributing to elevated levels of total organic composition (TOC) of the sediment. Increased TOC favors anaerobic respiration in marine sediments, and sulfide, a toxic by-product of this process, was found at levels as high as 17.5 mg L-1 in Thatcher Bay. The Thatcher Bay sulfide levels are several orders of magnitude higher than those known to impact benthic invertebrates.\r\n\r\nEelgrass, Zostera marina, located on the western margin of Thatcher Bay, was surveyed by using underwater video surveys. This baseline distribution will in part be used to measure the impact of any future remediation efforts. Additionally, the distribution and survey data can provide an estimate of propagule source for future colonization of restored sediment.\r\n\r\nThree restoration alternatives were considered, and a ranking matrix was developed to score each alternative against site-specific and regional criteria. The process identified the removal of wood-waste from a water-based platform as the preferred alternative.\r\n\r\nOur multidisciplinary investigation identified the location, thickness, and potential impacts of wood-waste that has persisted in the nearshore environment of Thatcher Bay since at least 1942. We also provide a process to efficiently evaluate alternatives to remediate the impact of this historical disturbance and to potentially contribute to an increase of nearshore diversity and productivity at this site. Elements of this approach could inform restoration planning at similarly impacted sites throughout the region.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20081369","collaboration":"Prepared for Skagit Fisheries Enhancement Group","usgsCitation":"Breems, J., Wyllie-Echeverria, S., Grossman, E., and Elliott, J., 2009, Thatcher Bay, Washington, Nearshore Restoration Assessment: U.S. Geological Survey Open-File Report 2008-1369, ix, 33 p., https://doi.org/10.3133/ofr20081369.","productDescription":"ix, 33 p.","costCenters":[{"id":645,"text":"Western Coastal and Marine Geology","active":false,"usgs":true}],"links":[{"id":125455,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2008_1369.jpg"},{"id":13071,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2008/1369/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -122.9,48.5 ], [ -122.9,48.6 ], [ -122.8,48.6 ], [ -122.8,48.5 ], [ -122.9,48.5 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad5e4b07f02db6836c5","contributors":{"authors":[{"text":"Breems, Joel","contributorId":35414,"corporation":false,"usgs":true,"family":"Breems","given":"Joel","email":"","affiliations":[],"preferred":false,"id":303527,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wyllie-Echeverria, Sandy","contributorId":24874,"corporation":false,"usgs":true,"family":"Wyllie-Echeverria","given":"Sandy","email":"","affiliations":[],"preferred":false,"id":303525,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Grossman, Eric E. 0000-0003-0269-6307 egrossman@usgs.gov","orcid":"https://orcid.org/0000-0003-0269-6307","contributorId":2334,"corporation":false,"usgs":true,"family":"Grossman","given":"Eric E.","email":"egrossman@usgs.gov","affiliations":[],"preferred":false,"id":303524,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Elliott, Joel","contributorId":34219,"corporation":false,"usgs":true,"family":"Elliott","given":"Joel","email":"","affiliations":[],"preferred":false,"id":303526,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":97882,"text":"ofr20091211 - 2009 - Low-fluorine Stockwork Molybdenite Deposits","interactions":[],"lastModifiedDate":"2018-10-29T10:50:15","indexId":"ofr20091211","displayToPublicDate":"2009-10-01T00:00:00","publicationYear":"2009","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":"2009-1211","title":"Low-fluorine Stockwork Molybdenite Deposits","docAbstract":"Low-fluorine stockwork molybdenite deposits are closely related to porphyry copper deposits, being similar in their tectonic setting (continental volcanic arc) and the petrology (calc-alkaline) of associated igneous rock types. They are mainly restricted to the Cordillera of western Canada and the northwest United States, and their distribution elsewhere in the world may be limited. The deposits consist of stockwork bodies of molybdenite-bearing quartz veinlets that are present in and around the upper parts of intermediate to felsic intrusions. The deposits are relatively low grade (0.05 to 0.2 percent Mo), but relatively large, commonly >50 million tons. The source plutons for these deposits range from granodiorite to granite in composition; the deposits primarily form in continental margin subduction-related magmatic arcs, often concurrent with formation of nearby porphyry copper deposits. Oxidation of pyrite in unmined deposits or in tailings and waste rock during weathering can lead to development of acid-rock drainage and limonite-rich gossans. Waters associated with low-fluorine stockwork molybdenite deposits tend to be nearly neutral in pH; variable in concentrations of molybdenum (<2 to >10,000 ug/L); below regulatory guidelines for copper, iron, lead, zinc, and mercury; and locally may exceed guidelines for arsenic, cadmium, and selenium.","language":"ENGLISH","publisher":"U.S. Geological Survey","doi":"10.3133/ofr20091211","usgsCitation":"Ludington, S., Hammarstrom, J., and Piatak, N.M., 2009, Low-fluorine Stockwork Molybdenite Deposits: U.S. Geological Survey Open-File Report 2009-1211, Available online and on CD-ROM, https://doi.org/10.3133/ofr20091211.","productDescription":"Available online and on CD-ROM","costCenters":[{"id":245,"text":"Eastern Mineral and Environmental Resources Science Center","active":true,"usgs":true},{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":125501,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/ofr_2009_1211.jpg"},{"id":13057,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/of/2009/1211/","linkFileType":{"id":5,"text":"html"}}],"geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -145,40 ], [ -145,65 ], [ -105,65 ], [ -105,40 ], [ -145,40 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a7fe4b07f02db6487f3","contributors":{"authors":[{"text":"Ludington, Steve","contributorId":106848,"corporation":false,"usgs":true,"family":"Ludington","given":"Steve","affiliations":[],"preferred":false,"id":303452,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hammarstrom, Jane","contributorId":55436,"corporation":false,"usgs":true,"family":"Hammarstrom","given":"Jane","affiliations":[],"preferred":false,"id":303451,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Piatak, Nadine M. 0000-0002-1973-8537 npiatak@usgs.gov","orcid":"https://orcid.org/0000-0002-1973-8537","contributorId":2324,"corporation":false,"usgs":true,"family":"Piatak","given":"Nadine","email":"npiatak@usgs.gov","middleInitial":"M.","affiliations":[],"preferred":false,"id":303450,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":97877,"text":"sir20095153 - 2009 - Hydrogeology and Ground-Water Flow in the Opequon Creek Watershed area, Virginia and West Virginia","interactions":[],"lastModifiedDate":"2024-03-05T12:10:33.414941","indexId":"sir20095153","displayToPublicDate":"2009-10-01T00:00:00","publicationYear":"2009","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":"2009-5153","title":"Hydrogeology and Ground-Water Flow in the Opequon Creek Watershed area, Virginia and West Virginia","docAbstract":"Due to increasing population and economic development in the northern Shenandoah Valley of Virginia and West Virginia, water availability has become a primary concern for water-resource managers in the region. To address these issues, the U.S. Geological Survey (USGS), in cooperation with the West Virginia Department of Health and Human Services and the West Virginia Department of Environmental Protection, developed a numerical steady-state simulation of ground-water flow for the 1,013-square-kilometer Opequon Creek watershed area. The model was based on data aggregated for several recently completed and ongoing USGS hydrogeologic investigations conducted in Jefferson, Berkeley, and Morgan Counties in West Virginia and Clarke, Frederick, and Warren Counties in Virginia. A previous detailed hydrogeologic assessment of the watershed area of Hopewell Run (tributary to the Opequon Creek), which includes the USGS Leetown Science Center in Jefferson County, West Virginia, provided key understanding of ground-water flow processes in the aquifer.\r\n\r\nThe ground-water flow model developed for the Opequon Creek watershed area is a steady-state, three-layer representation of ground-water flow in the region. The primary objective of the simulation was to develop water budgets for average and drought hydrologic conditions. The simulation results can provide water managers with preliminary estimates on which water-resource decisions may be based.\r\n\r\nResults of the ground-water flow simulation of the Opequon Creek watershed area indicate that hydrogeologic concepts developed for the Hopewell Run watershed area can be extrapolated to the larger watershed model. Sensitivity analyses conducted as part of the current modeling effort and geographic information system analyses of spring location and yield reveal that thrust and cross-strike faults and low-permeability bedding, which provide structural and lithologic controls, respectively, on ground-water flow, must be incorporated into the model to develop a realistic simulation of ground-water flow in the larger Opequon Creek watershed area.\r\n\r\nIn the model, recharge for average hydrologic conditions was 689 m3/d/km2 (cubic meters per day per square kilometer) over the entire Opequon Creek watershed area. Mean and median measured base flows at the streamflow-gaging station on the Opequon Creek near Martinsburg, West Virginia, were 604,384 and 349,907 m3/d (cubic meters per day), respectively. The simulated base flow of 432,834 m3/d fell between the mean and median measured stream base flows for the station. Simulated base-flow yields for subwatersheds during average conditions ranged from 0 to 2,643 m3/d/km2, and the median for the entire Opequon Creek watershed area was 557 m3/d/km2.\r\n\r\nA drought was simulated by reducing model recharge by 40 percent, a rate that approximates the recharge during the prolonged 16-month drought that affected the region from November 1998 to February 2000. Mean and median measured streamflows for the Opequon Creek watershed area at the Martinsburg, West Virginia, streamflow-gaging station during the 1999 drought were 341,098 and 216,551 m3/d, respectively. The simulated drought base flow at the station of 252,356 m3/d is within the range of flows measured during the 1999 drought. Recharge was 413 m3/d/km2 over the entire watershed during the simulated drought, and was 388 m3/d/km2 at the gaging station. Simulated base-flow yields for drought conditions ranged from 0 to 1,865 m3/d/km2 and averaged 327 m3/d/km2 over the entire Opequon Creek watershed.\r\n\r\nWater budgets developed from the simulation results indicate a substantial component of direct ground-water discharge to the Potomac River. This phenomenon had long been suspected but had not been quantified. During average conditions, approximately 564,176 m3/d of base flow discharges to the Potomac River. An additional 124,379 m3/d of ground water is also estimated to discharge directly to the Potomac River and rep","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/sir20095153","collaboration":"Prepared in cooperation with the West Virginia Department of Health and Human Services and the West Virginia Department of Environmental Protection","usgsCitation":"Kozar, M.D., and Weary, D.J., 2009, Hydrogeology and Ground-Water Flow in the Opequon Creek Watershed area, Virginia and West Virginia: U.S. Geological Survey Scientific Investigations Report 2009-5153, vi, 63 p., https://doi.org/10.3133/sir20095153.","productDescription":"vi, 63 p.","temporalStart":"1998-11-01","temporalEnd":"2000-02-28","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true},{"id":50464,"text":"Eastern Ecological Science Center","active":true,"usgs":true}],"links":[{"id":118456,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/sir_2009_5153.jpg"},{"id":13052,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/sir/2009/5153/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4de4b07f02db627839","contributors":{"authors":[{"text":"Kozar, Mark D. 0000-0001-7755-7657 mdkozar@usgs.gov","orcid":"https://orcid.org/0000-0001-7755-7657","contributorId":1963,"corporation":false,"usgs":true,"family":"Kozar","given":"Mark","email":"mdkozar@usgs.gov","middleInitial":"D.","affiliations":[{"id":37280,"text":"Virginia and West Virginia Water Science Center ","active":true,"usgs":true}],"preferred":true,"id":303432,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Weary, David J. 0000-0002-6115-6397 dweary@usgs.gov","orcid":"https://orcid.org/0000-0002-6115-6397","contributorId":545,"corporation":false,"usgs":true,"family":"Weary","given":"David","email":"dweary@usgs.gov","middleInitial":"J.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true},{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":303431,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}