The Wilderness Act (Public Law 88-577, September 3, 1964) and related acts require the U.S. Geological Survey and the U.S. Bureau of Mines to survey certain areas on Federal lands to determine their mineral value, if any, that may be present. Results must be made available to the public and be submitted to the President and the Congress. This report presents the results of investigations of mines, prospects, and mineral sites in the Great Gulf and Presidential Range-Dry River Wilderness Areas; the Dartmouth Range, Wild River, Pemigewasset, Kinsman Mountain, Mount Wolf-Gordon Pond, Jobildunk, and Carr Mountain Roadless Areas; and the intervening and immediately surrounding areas in the White Mountain National Forest, Coos, Grafton, and Carroll Counties, New Hampshire. The Great Gulf Wilderness was established when the Wilderness Act was passed in 1964, and the Presidential Range-Dry River Wilderness was established by Public Law 93-622, January 3, 1975. The Dartmouth Range, Wild River, Pemigewasset, Kinsman Mountain, Mount Wolf-Gordon Pond, Carr Mountain, and Jobildunk areas were classified as a further planning area during the Second Roadless Area Review and Evaluation (RARE II) by the U.S. Forest Service, January 1979.
\nThe areas investigated are located in the White Mountain National Forest in Coos, Grafton, and Carroll Counties, New Hampshire. Personnel from the U.S. Bureau of Mines conducted field reconnaissance of the westernmost areas, Kinsman Mountain, Mt. Wolf-Gordon Pond, Jobildunk, and Carr Mountain, in the fall of 1980. Field reconnaissance of the eastern areas, Great Gulf, Presidential Range-Dry River, Dartmouth Range, Pemigewasset and Wild River was conducted in the spring of 1981. A total of 237 rock and 103 panned-concentrate samples were collected during the investigations. Reconnaissance radiometric ground surveys were conducted at selected locations.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf1594E","usgsCitation":"Gazdik, G.C., Harris, G., Welsh, R.A., and Girol, V.P., 1988, Mines, prospects, and mineral sites, wilderness and RARE II areas, White Mountain National Forest, New Hampshire: U.S. Geological Survey Miscellaneous Field Studies Map 1594-E, 2 Plates: 54.42 x 39.82 inches and 22.71 x 28.02 inches, https://doi.org/10.3133/mf1594E.","productDescription":"2 Plates: 54.42 x 39.82 inches and 22.71 x 28.02 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":326382,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/mf1594E.PNG"},{"id":327604,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1594-E/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":327605,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1594-E/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"125000","country":"United States","state":"New Hampshire","county":"Carroll County, Coos County, Grafton County","otherGeospatial":"White Mountain National Forest","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -72,\n 43.75\n ],\n [\n -72,\n 44.75\n ],\n [\n -70.75,\n 44.75\n ],\n [\n -70.75,\n 43.75\n ],\n [\n -72,\n 43.75\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699d5f","contributors":{"authors":[{"text":"Gazdik, G. C.","contributorId":119969,"corporation":false,"usgs":true,"family":"Gazdik","given":"G.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":511915,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Harris, Gazdik","contributorId":46610,"corporation":false,"usgs":true,"family":"Harris","given":"Gazdik","email":"","affiliations":[],"preferred":false,"id":511912,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Welsh, R. A.","contributorId":117076,"corporation":false,"usgs":true,"family":"Welsh","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":511913,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Girol, V. P.","contributorId":117406,"corporation":false,"usgs":true,"family":"Girol","given":"V.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":511914,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":38632,"text":"pp1049F - 1988 - Geology and resources of thorium and associated elements in the Wet Mountains area, Fremont and Custer counties, Colorado","interactions":[],"lastModifiedDate":"2012-02-02T00:10:35","indexId":"pp1049F","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"1049","chapter":"F","title":"Geology and resources of thorium and associated elements in the Wet Mountains area, Fremont and Custer counties, Colorado","docAbstract":"Thorium in potentially economic amounts occurs in three types of deposits in the Wet Mountains area of Colorado: (1) quartz-baritethorite veins and fracture zones, (2) carbonatite dikes, and (3) red syenite dikes. The quartz-barite-thorite veins and fracture zones contain the largest resources of thorium; they cut all Precambrian and Paleozoic rock types in the area and tend to strike normal to the foliation in the Proterozoic metasedimentary and metavolcanic rocks. The veins and fracture zones are end products of the episode of Cambrian alkaline magmatism that also produced rocks of the McClure Mountain Complex, the Gem Park Complex, the complex at Democrat Creek, and associated dikes of carbonatite, lamprophyre, and red syenite. The veins and fracture zones contain an average of 0.46 percent ThO2, 0.21 percent SLREE (total light rare-earth elements), 0.14 percent SHREE (total heavy rare-earth elements), and 0.012 percent Nb2O5; They contain reserves of 64,200 tons ThO2, 29,300 tons SLREE, 19,540 tons SHREE, 1,675 tons Nb2O5; they contain probable potential resources of 160,500 tons ThO2, 73,270 tons SLREE, 48,850 tons SHREE, and 4,185 tons Nb2O5. \r\n\r\nThe carbonatite dikes form two distinct groups: replacement carbonatites and primary magmatic carbonatites. The latter group appears to be the better source of potentially economic commodities. The primary magmatic carbonatites contain an average of 0.17 percent ThO2, 0.0097 percent Nb2O5, 0.0031 percent U3O5, and 2.15 percent total rare-earth oxides. The seven largest dikes contain reserves of 131 tons ThO2, 40 tons Nb2O5, 17 tons U3O5, and 2,500 tons SRE203 (total rare-earth oxides), and probable potential resources of 753 tons ThO2, 228 tons Nb2O5, 105 tons U3O5, and 14,300 tons SRE2O3.\r\n\r\nThe red syenite dikes contain anomalous amounts of thorium, uranium, niobium, and rare-earth elements. Although reserves and probable potential resources have not been calculated, they are likely to be small.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Geology and resources of thorium in the United States","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"ENGLISH","doi":"10.3133/pp1049F","usgsCitation":"Armbrustmacher, T., 1988, Geology and resources of thorium and associated elements in the Wet Mountains area, Fremont and Custer counties, Colorado: U.S. Geological Survey Professional Paper 1049, p. F1-F34, 1 plate in pocket, https://doi.org/10.3133/pp1049F.","productDescription":"p. F1-F34, 1 plate in pocket","costCenters":[],"links":[{"id":104543,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4704.htm","linkFileType":{"id":5,"text":"html"},"description":"4704"},{"id":124512,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/1049f/report-thumb.jpg"},{"id":65459,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/1049f/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":65460,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/1049f/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b46db","contributors":{"authors":[{"text":"Armbrustmacher, T.J.","contributorId":92642,"corporation":false,"usgs":true,"family":"Armbrustmacher","given":"T.J.","affiliations":[],"preferred":false,"id":220192,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":12803,"text":"ofr889 - 1988 - Plotting programs for rare earth elements, spider diagrams, and ternary diagrams","interactions":[],"lastModifiedDate":"2012-02-02T00:06:55","indexId":"ofr889","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"88-9","title":"Plotting programs for rare earth elements, spider diagrams, and ternary diagrams","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr889","usgsCitation":"Bruggman, P., 1988, Plotting programs for rare earth elements, spider diagrams, and ternary diagrams: U.S. Geological Survey Open-File Report 88-9, i, 17 p. :ill. ;28 cm.; 5.25 inch diskette, https://doi.org/10.3133/ofr889.","productDescription":"i, 17 p. :ill. ;28 cm.; 5.25 inch diskette","costCenters":[],"links":[{"id":146853,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1988/0009/report-thumb.jpg"},{"id":41217,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1988/0009/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db684d87","contributors":{"authors":[{"text":"Bruggman, P. E.","contributorId":83536,"corporation":false,"usgs":true,"family":"Bruggman","given":"P. E.","affiliations":[],"preferred":false,"id":166743,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":27757,"text":"wri884122 - 1988 - Review of mechanisms, methods, and theory for determining recharge to shallow aquifers in North Dakota","interactions":[],"lastModifiedDate":"2018-03-08T13:08:25","indexId":"wri884122","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":342,"text":"Water-Resources Investigations Report","code":"WRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"88-4122","title":"Review of mechanisms, methods, and theory for determining recharge to shallow aquifers in North Dakota","docAbstract":"Effective management of ground-water resources requires knowledge of all components of the water budget for the aquifer of interest. Efforts to simulate ground-water flow prior to development and the effects of proposed pumping in several of North Dakota's shallow glacial aquifers have been hindered by the lack of reliable estimates of ground-water recharge. This study was done to (1) review the methods that have been used to measure recharge, (2) review the theory of unsaturated flow and the methods for characterizing the physical properties of unsaturated media, (3) consider the relative merits of a rigorous data-intensive approach versus an estimation approach to the study of recharge, and (4) review past and current agronomic research in North Dakota for applicability of the research and the data generated to the study of recharge.
Direct, quantitative techniques for evaluating recharge are rarely applied. The theory for computing fluxes in unsaturated media is well established and numerous physics-based models that effectively implement the theory are available, but the data required for the models generally are lacking. Many parametric approaches have been developed to avoid the large data requirements of the physics-based approaches for analyzing flow in the unsaturated zone. However, the parametric approaches normally include fitting coefficients that must be calibrated for every study site, thereby detracting from the general utility of the parametric approach.
The functional relation of matric potential to moisture content is required for physics-based soil-water models, whether analytic or numeric. Laboratory methods to determine these relations are tedious, costly, and may not give results representative of the soils as they occur in the field. Many models have been proposed to estimate the moisture-characteristic curve and hydraulic-conductivity function from basic soil properties, but none yield results that are universally satisfactory. In situ methods, because they require minimal disturbance of the soil profile and may be used repeatedly on the same soil mass, have become the preferred means for acquiring physical data, especially hydraulic conductivity. Hydro logic investigations, except for recent studies of hazardous-waste disposal sites, rarely have included physical characterizations of unsaturated media.
Any of four phenomena could hinder attempts to simulate unsaturated flow in settings typical of North Dakota; variability of soil properties, hysteresis, frozen ground, and macropore development. The spatial and temporal variability of soil properties probably is the greatest complicating phenomenon and must be dealt with by detailed characterization of the properties. Hysteresis can detract from the accuracy of flow calculations for some soils under certain conditions but, for the present, our scant knowledge of soil physical properties is a greater hindrance to reliable soi1-water mode 1 ing than is the hysteresis phenomenon. A1 though seasona1ly frozen ground undoubtedly affects hydrologic processes in North Dakota, much more research is needed before meaningful quantitative treatment is possible. Finally, macropores can influence soil-water movement significantly, but macropore development may not be common on the intensively farmed, coarse-textured soils that typically overlie North Dakota's glacial aquifers. Lysimetry currently is the only reliable means of analyzing macropore flow.
The soil-related research that has been conducted in North Dakota to date (1983) provides little of the type of information required to estimate ground-water recharge. Useful data could be developed by systematically evaluating the hydraulic characteristics of the prominent soil types overlying North Dakota's shallow glacial aquifers. These data would be required to enable use of a physics-based approach to estimating recharge. The size of the aquifer under study, its economic value, and the resources available for data collection should be considered when choosing between parametric or physics-based methods.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri884122","usgsCitation":"Horak, W., 1988, Review of mechanisms, methods, and theory for determining recharge to shallow aquifers in North Dakota: U.S. Geological Survey Water-Resources Investigations Report 88-4122, iv, 54 p., https://doi.org/10.3133/wri884122.","productDescription":"iv, 54 p.","costCenters":[{"id":478,"text":"North Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":157960,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1988/4122/report-thumb.jpg"},{"id":56604,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1988/4122/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1ae4b07f02db6a80f4","contributors":{"authors":[{"text":"Horak, W.F.","contributorId":82326,"corporation":false,"usgs":true,"family":"Horak","given":"W.F.","email":"","affiliations":[],"preferred":false,"id":198648,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13526,"text":"ofr88566 - 1988 - Trace element and rare earth element variation in fluorites collected from skarn and epithermal mineral deposits in the Sierra Cuchillo area, south-central New Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:06:44","indexId":"ofr88566","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","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":"88-566","title":"Trace element and rare earth element variation in fluorites collected from skarn and epithermal mineral deposits in the Sierra Cuchillo area, south-central New Mexico","language":"ENGLISH","publisher":"U.S. Geological Survey,","doi":"10.3133/ofr88566","usgsCitation":"Eppinger, R., 1988, Trace element and rare earth element variation in fluorites collected from skarn and epithermal mineral deposits in the Sierra Cuchillo area, south-central New Mexico: U.S. Geological Survey Open-File Report 88-566, 108 p. ill., maps ;28 cm., https://doi.org/10.3133/ofr88566.","productDescription":"108 p. ill., maps ;28 cm.","costCenters":[],"links":[{"id":145329,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1988/0566/report-thumb.jpg"},{"id":42003,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1988/0566/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42004,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1988/0566/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42005,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1988/0566/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a4ee4b07f02db627eb9","contributors":{"authors":[{"text":"Eppinger, R. G.","contributorId":100837,"corporation":false,"usgs":true,"family":"Eppinger","given":"R. G.","affiliations":[],"preferred":false,"id":167948,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":60361,"text":"mf1921A - 1988 - Mineral resource potential map of the Pecos Wilderness, Santa Fe, San Miguel, Mora, Rio Arriba, and Taos Counties, New Mexico","interactions":[],"lastModifiedDate":"2025-05-23T18:51:56.04573","indexId":"mf1921A","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1921","chapter":"A","title":"Mineral resource potential map of the Pecos Wilderness, Santa Fe, San Miguel, Mora, Rio Arriba, and Taos Counties, New Mexico","docAbstract":"The Pecos Wilderness covers approximately 348 sq mi in the Santa Fe and Carson National Forests, north-central New Mexico. The area investigated includes the wilderness and approximately 150 sq mi of adjacent territory. The additional area covers several RARE II Road less Areas that were classified by the U.S. Forest Service in 1979 as Proposed Wilderness and Further Planning Areas, but were not incorporated in the Pecos Wilderness by the New Mexico Wilderness Bill. For the purpose of this report the entire area is called the study area.
\nThe study area is at the southern end of the Sangre de Cristo Range. It is characterized by an axial line of alpine peaks that rise to more than 13,000 ft, flanked on the west and north by heavily wooded ridges and canyons that drain to the Rio Grande Valley, and on the southeast by a high dissected plateau of meadows and forest. The plateau is dissected by deep canyons of the Pecos River and its tributaries, and is bounded on the east by a scarp of about 3,000 ft. Partly forested ranch land lies below the base of the scarp to the east, and beyond that is prai-rie of the Great Plains.
\nThis map is based on geologic and geochemical studies and mine and prospect investigations that were done principally in 1977 and 1979-80 (U.S. Geological Survey, U.S. Bureau of Mines, and New Mexico Bureau of Mines and Mineral Resources, 1980; Lane, 1980; Moench and Robertson, 1980; Moench, Robertson, and Sutley, 1980; Moench and Erickson, 1980; Moench, Grambling, and Robertson, 1988; Moench, Sutley, and Erickson, 1988; Erickson, Sutley, and Moench, 1986). An aeromagnetic survey covering almost all of the Pecos Wilderness was flown in 1970. The resulting aeromagnetic map was published by Moench and others (1980) and interpreted in that report by Lindreth Cordell. Cordell found no correlation between magnetic features and geologic terraines having mineral resource potential.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/mf1921A","usgsCitation":"Moench, R.H., and Lane, M.E., 1988, Mineral resource potential map of the Pecos Wilderness, Santa Fe, San Miguel, Mora, Rio Arriba, and Taos Counties, New Mexico: U.S. Geological Survey Miscellaneous Field Studies Map 1921, Report: 15 p.; 1 Plate: 39.17 x 56.44 inches, https://doi.org/10.3133/mf1921A.","productDescription":"Report: 15 p.; 1 Plate: 39.17 x 56.44 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":327363,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/1921-A/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":88790,"rank":3,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/mf/1988/1921a/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":183202,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/1988/1921a/report-thumb.jpg"},{"id":407322,"rank":2,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_5486.htm","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"New Mexico","county":"Mora County, Rio Arriba County, San Miguel County, Santa Fe County, Taos County","otherGeospatial":"Pecos Wilderness","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.875,\n 35.6008\n ],\n [\n -105.3906,\n 35.6008\n ],\n [\n -105.3906,\n 36.1039\n ],\n [\n -105.875,\n 36.1039\n ],\n [\n -105.875,\n 35.6008\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fae4b07f02db5f4132","contributors":{"authors":[{"text":"Moench, R. H.","contributorId":8853,"corporation":false,"usgs":true,"family":"Moench","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":263607,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lane, M. E.","contributorId":9262,"corporation":false,"usgs":true,"family":"Lane","given":"M.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":263608,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70156297,"text":"70156297 - 1988 - Phytoplankton growth rates in a light-limited environment, San Francisco Bay","interactions":[],"lastModifiedDate":"2018-09-12T16:19:01","indexId":"70156297","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2663,"text":"Marine Ecology Progress Series","active":true,"publicationSubtype":{"id":10}},"title":"Phytoplankton growth rates in a light-limited environment, San Francisco Bay","docAbstract":"Phytoplankton cells reside in a turbulent medium partitioned into an upper photic zone that sustains photosynthesis, and a lower aphotic zone that does not. In estuaries, vertical mixing rates between these 2 zones can be rapid (< 1 generation time) because of tidal stirring and because the mixing depth is generally shallow. Moreover, the photic depth is characteristically shallow in estuaries because of the high seston concentrations that typify these systems (e.g. Cloern 1987). Hence the mean light exposure of phytoplankton cells, and their rates of photosynthesis and growth in estuaries, should be related to the ratio of photic depth Zp to mixing Zm, (defined as either the water column depth, or the surface layer depth in a stratified estuary).
\nGrobbelar (1985) has measured phytoplankton production in turbid waters and used the ratio Zp:Zm as a simple index to quantify the degree of light limitation. Harris and his colleagues have examined in detail the importance of the Zp:Zm ratio in lakes for influencing variability of phytoplankton production and photosynthetic parameters (Harris et al. 1980), and variability of species composition both temporally (Harris & Piccinin 1980) and spatially (Haffner et al. 1980). Phytoplankton growth rates have only rarely been measured in estuaries (Malone 1977, Furnas 1982, Harding et al. 1986) where cycling rates between the photic and aphotic zones can be much faster than in lakes or the open ocean.
\nThis study was motivated by the need for quantitative measures of phytoplankton population growth rate in an estuarine environment, and was designed around the presumption that growth rates can be related empirically to light exposure. We conducted the study in San Francisco Bay (California, USA), which has large horizontal gradients in light availability (Zp:Zm) typical of many coastal plain estuaries, and nutrient concentrations that often exceed those presumed to limit phytoplankton growth (Cloern et al. 1985). We tested the hypothesis that light availability is the primary control of phytoplankton growth, and that previous estimates of growth rate based on the ratio of productivity to biomass (Cloern et al. 1985) are realistic. Specifically, we wanted to verify that growth rate varies spatially along horizontal gradients of light availability indexed as Zp:Zm, such that phytoplankton turnover rate is rapid in shallow clear areas (high Zp:Zm) and slow in deep turbid areas (low Zp:Zm). We used an in situ incubation technique which simulated vertical mixing, and measured both changes in cell number and carbon production as independent estimates of growth rate across a range of Zp:Zm ratios.
","publisher":"Inter-Research","usgsCitation":"Alpine, A.E., and Cloern, J.E., 1988, Phytoplankton growth rates in a light-limited environment, San Francisco Bay: Marine Ecology Progress Series, v. 44, p. 167-173.","productDescription":"7 p.","startPage":"167","endPage":"173","numberOfPages":"7","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true},{"id":552,"text":"San Francisco Bay-Delta","active":false,"usgs":true}],"links":[{"id":306911,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":306910,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.int-res.com/abstracts/meps/v44/"}],"country":"United States","state":"California","city":"San Francisco","otherGeospatial":"San Francisco Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.54974365234374,\n 37.43125050179356\n ],\n [\n -122.54974365234374,\n 38.16047628099622\n ],\n [\n -121.9647216796875,\n 38.16047628099622\n ],\n [\n -121.9647216796875,\n 37.43125050179356\n ],\n [\n -122.54974365234374,\n 37.43125050179356\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"44","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"55d5a8b2e4b0518e3546a4d7","contributors":{"authors":[{"text":"Alpine, Andrea E.","contributorId":54927,"corporation":false,"usgs":true,"family":"Alpine","given":"Andrea","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":568550,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cloern, James E. 0000-0002-5880-6862 jecloern@usgs.gov","orcid":"https://orcid.org/0000-0002-5880-6862","contributorId":1488,"corporation":false,"usgs":true,"family":"Cloern","given":"James","email":"jecloern@usgs.gov","middleInitial":"E.","affiliations":[{"id":438,"text":"National Research Program - Western Branch","active":true,"usgs":true},{"id":37277,"text":"WMA - Earth System Processes Division","active":true,"usgs":true}],"preferred":true,"id":568551,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70122708,"text":"70122708 - 1988 - Conservation of North American rallids","interactions":[],"lastModifiedDate":"2014-08-27T13:37:22","indexId":"70122708","displayToPublicDate":"1988-09-01T13:19:56","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3783,"text":"The Wilson Bulletin","printIssn":"0043-5643","active":true,"publicationSubtype":{"id":10}},"title":"Conservation of North American rallids","docAbstract":"The Rallidae are a diverse group in their habitat selection, yet most North American species occur in or near wetlands As a consequence, most species are subject to habitat enhancement or perturbation from waterfowl management programs. The overall effects of these management programs relative to rallid conservation have been assessed for few species, and there is a need for synthesis of such information. In the cases of some species or raves, population status is not known, and suggested directions for conservation and management are needed. Rare, endangered, or status undetermined species or races often occur in areas where related species are classified as game birds, and the effects of such hunting on rarer forms are not known. Their generally secretive nature, the endangered status of several races and populations, and continued loss of habitat and threats to present habitat, warrant an examination of the conservation status of the North American taxa in this group.
\nIn 1977, a committee of the International Association of Fish and Wildlife Agencies summarized available information on management and biology of American Coots (Fulica americana), rails, and gallinules in North America (Holliman 1977). That summary was intended to provide relatively complete information on conservation of these species, and also to provide guidance for research within the U.S. Fish and Wildlife Service's (FWS) Accelerated Research Program for Webless Migratory Shore and Upland Game Birds (ARP). Subsequently, a number of rallid studies were funded under this program. The program was eliminated in 1982, following substantial research activities on North American rallids.
\nSince the demise of the ARP, additional research on rallids in North America has focused on an area the International Association of Fish and Wildlife Agencies report failed to cover in detail--that of endangered rallids in the U.S. and their possessions. Most of these studies have been of threatened and endangered taxa in western coastal marshes. This report updates and summarizes information on North American rallids since the ARP report and identifies the major conservation problems of this group with the intent of focusing future efforts on these priority issues. Consideration of island forms occurring within U.S. possessions is beyond the scope of this report, mainly because of the special conservation problems associated with their insular distribution. The major topics include habitat requirements, effects of habitat and hunting management techniques currently practiced on wetland areas, and conservation of endangered and threatened populations. Research needs are identified. Habitats of the American Coot are similar to those of several waterfowl species, and the biology of coots is considered only as it is typical of rails in general.
","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Wilson Bulletin","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"Wilson Ornithological Society","publisherLocation":"Lawrence, KS","usgsCitation":"Eddleman, W.R., Knopf, F., Manley, B., Reid, F.A., and Zembal, R., 1988, Conservation of North American rallids: The Wilson Bulletin, v. 100, no. 3, p. 458-475.","productDescription":"17 p.","startPage":"458","endPage":"475","numberOfPages":"17","costCenters":[],"links":[{"id":293129,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"100","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53fef0d1e4b01f35f8fd695e","contributors":{"authors":[{"text":"Eddleman, William R.","contributorId":40685,"corporation":false,"usgs":true,"family":"Eddleman","given":"William","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":499651,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Knopf, Fritz L.","contributorId":30549,"corporation":false,"usgs":true,"family":"Knopf","given":"Fritz L.","affiliations":[{"id":291,"text":"Fort Collins Science Center","active":true,"usgs":true}],"preferred":false,"id":499648,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Manley, Brooke","contributorId":21474,"corporation":false,"usgs":true,"family":"Manley","given":"Brooke","email":"","affiliations":[],"preferred":false,"id":499647,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Reid, Frederic A.","contributorId":33235,"corporation":false,"usgs":true,"family":"Reid","given":"Frederic","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":499649,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Zembal, Richard","contributorId":38482,"corporation":false,"usgs":true,"family":"Zembal","given":"Richard","affiliations":[],"preferred":false,"id":499650,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70013302,"text":"70013302 - 1988 - A new Lower Carboniferous tetrapod locality in Iowa","interactions":[],"lastModifiedDate":"2025-06-02T16:25:20.210733","indexId":"70013302","displayToPublicDate":"1988-06-23T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"A new Lower Carboniferous tetrapod locality in Iowa","docAbstract":"The earliest tetrapods known are from two or three Upper Devonian1–3 and some 20 Lower Carboniferous localities in Scotland4 and North America5–8. Most sites yield few and fragmentary specimens; well-preserved and even partially articulated material is exceedingly rare. This report discusses a middle Lower Carboniferous site rich in amphibian and fish remains discovered near Delta, south-east Iowa, and represents the first Lower Carboniferous tetrapod locality found in mid-continental North America. The bones occur within collapse-structures or depressions, and appear to represent a fresh- or brackish-water pond fauna. The Delta site contains the oldest well-preserved tetrapod fauna in North America, and one of the oldest in the world. Several hundred tetrapod fossils have been collected to date, with excavation somewhat more than half completed. Specimens range from isolated bones to articulated, nearly complete skeletons of at least two apparently new amphibian species. This material will make an important contribution to knowledge of the mor-phology and interrelationships of early tetrapods.
","language":"English","publisher":"Springer Nature","doi":"10.1038/333768a0","issn":"00280836","usgsCitation":"Bolt, J., McKay, R., Witzke, B., and McAdams, M., 1988, A new Lower Carboniferous tetrapod locality in Iowa: Nature, v. 333, no. 6175, p. 768-770, https://doi.org/10.1038/333768a0.","productDescription":"3 p.","startPage":"768","endPage":"770","costCenters":[],"links":[{"id":220299,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Iowa","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -96.69321098034271,\n 43.54256954893344\n ],\n [\n -96.72858624817624,\n 42.73699803843523\n ],\n [\n -96.1161908673356,\n 41.780553985192824\n ],\n [\n -95.90624885835399,\n 40.48760168558948\n ],\n [\n -91.92848582950946,\n 40.58236406842123\n ],\n [\n -91.4363674865877,\n 40.29164457407646\n ],\n [\n -90.90527191776219,\n 40.891384940468015\n ],\n [\n -90.09462276356368,\n 41.90527987432017\n ],\n [\n -90.63381627372756,\n 42.729413795212736\n ],\n [\n -91.24190728304254,\n 43.53316060224191\n ],\n [\n -96.69321098034271,\n 43.54256954893344\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"333","issue":"6175","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e499e4b0c8380cd46758","contributors":{"authors":[{"text":"Bolt, J.R.","contributorId":57205,"corporation":false,"usgs":true,"family":"Bolt","given":"J.R.","email":"","affiliations":[],"preferred":false,"id":365762,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McKay, R.M.","contributorId":91238,"corporation":false,"usgs":true,"family":"McKay","given":"R.M.","email":"","affiliations":[],"preferred":false,"id":365764,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Witzke, B.J.","contributorId":12976,"corporation":false,"usgs":true,"family":"Witzke","given":"B.J.","affiliations":[],"preferred":false,"id":365761,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"McAdams, M.P.","contributorId":81633,"corporation":false,"usgs":true,"family":"McAdams","given":"M.P.","email":"","affiliations":[],"preferred":false,"id":365763,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70014290,"text":"70014290 - 1988 - Uranium-series dating of the Mousterian occupation at Abric Romani, Spain","interactions":[],"lastModifiedDate":"2025-06-02T16:36:01.712608","indexId":"70014290","displayToPublicDate":"1988-03-03T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Uranium-series dating of the Mousterian occupation at Abric Romani, Spain","docAbstract":"The precise evolutionary position of the Neanderthal people continues to be a major uncertainty in human evolution. Their origin and their relationship to anatomically modern people are unclear and are clouded by poor chronology. Lithic artefacts of the Mousterian type, found throughout Europe and the Mediterranean Basin, are believed to be the tool kit of the Neanderthals, but dates within Mousterian-bearing deposits are extremely rare. We report here on 20 high-quality uranium-series dates from Mousterian beds at Abric Romani, a rock shelter near Barcelona, Spain. The dates range from 39 to 60 kyr before present (BP) in an orderly stratigraphic succession and provide precise chronological control on an important Mousterian archaeological site.
","language":"English","publisher":"Springer Nature","doi":"10.1038/332068a0","issn":"00280836","usgsCitation":"Bischoff, J.L., Julia, R., and Mora, R., 1988, Uranium-series dating of the Mousterian occupation at Abric Romani, Spain: Nature, v. 332, no. 6159, p. 68-70, https://doi.org/10.1038/332068a0.","productDescription":"3 p.","startPage":"68","endPage":"70","costCenters":[],"links":[{"id":226013,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Spain","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n 0.7394803397147314,\n 41.42726915584606\n ],\n [\n 0.7394803397147314,\n 40.94158367368533\n ],\n [\n 2.131767791876058,\n 40.94158367368533\n ],\n [\n 2.131767791876058,\n 41.42726915584606\n ],\n [\n 0.7394803397147314,\n 41.42726915584606\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"332","issue":"6159","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bbdffe4b08c986b329359","contributors":{"authors":[{"text":"Bischoff, J. L.","contributorId":28969,"corporation":false,"usgs":true,"family":"Bischoff","given":"J.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":368048,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Julia, R.","contributorId":34655,"corporation":false,"usgs":true,"family":"Julia","given":"R.","email":"","affiliations":[],"preferred":false,"id":368049,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mora, R.","contributorId":60392,"corporation":false,"usgs":true,"family":"Mora","given":"R.","email":"","affiliations":[],"preferred":false,"id":368050,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014327,"text":"70014327 - 1988 - Granulite fades Nd-isotopic homogenization in the Lewisian complex of northwest Scotland","interactions":[],"lastModifiedDate":"2025-06-02T16:41:20.325511","indexId":"70014327","displayToPublicDate":"1988-02-25T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Granulite fades Nd-isotopic homogenization in the Lewisian complex of northwest Scotland","docAbstract":"A published Sm–Nd whole-rock isochron of 2,920 ± 50 Myr, obtained from a wide range of lithologies in the Lewisian complex of north-west Scotland, was interpreted1 as the time of protolith formation. This date is ∼260 Myr older than estimates for the timing of high-grade metamorphism in the complex at ∼ 2,660 Myr2'3, and this period is considered to represent the duration of the Lewisian crustal accretion-differentiation superevent (CADS)4. Here we give new Sm-Nd data, obtained specifically from granulite facies tonalitic gneisses, that yield a date of 2,600 ±155 Myr. Although depleted-mantle model ages (tDM suggest >200 Myr of premetamorphic crustal residence, the regression date and its associated initial Nd-isotopic parameters demonstrate Nd-isotopic homogenization during the high-grade event, as well as the probability of general rare-earth-element (REE) mobility. Models for selective element depletion in the complex have previously assumed REE immobility since 2,920 Myr, but the data presented here suggest that a reappraisal of the depletion mechanism is required.
","language":"English","publisher":"Springer Nature","doi":"10.1038/331705a0","issn":"00280836","usgsCitation":"Whitehouse, M., 1988, Granulite fades Nd-isotopic homogenization in the Lewisian complex of northwest Scotland: Nature, v. 331, no. 6158, p. 705-707, https://doi.org/10.1038/331705a0.","productDescription":"3 p.","startPage":"705","endPage":"707","costCenters":[],"links":[{"id":225566,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Scotland","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -7.80190488310231,\n 58.5924285295051\n ],\n [\n -7.80190488310231,\n 56.07473135845302\n ],\n [\n -3.853372128121464,\n 56.07473135845302\n ],\n [\n -3.853372128121464,\n 58.5924285295051\n ],\n [\n -7.80190488310231,\n 58.5924285295051\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"331","issue":"6158","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a29c7e4b0c8380cd5ac20","contributors":{"authors":[{"text":"Whitehouse, M.J.","contributorId":87699,"corporation":false,"usgs":true,"family":"Whitehouse","given":"M.J.","email":"","affiliations":[],"preferred":false,"id":368128,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70013813,"text":"70013813 - 1988 - Fluid inclusions in vadose cement with consistent vapor to liquid ratios, Pleistocene Miami Limestone, southeastern Florida","interactions":[],"lastModifiedDate":"2024-04-03T16:11:14.614081","indexId":"70013813","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1759,"text":"Geochimica et Cosmochimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Fluid inclusions in vadose cement with consistent vapor to liquid ratios, Pleistocene Miami Limestone, southeastern Florida","docAbstract":"Vadose cements in the Late Pleistocene Miami Limestone contain regions with two-phase aqueous fluid inclusions that have consistent vapor to liquid (V-L) ratios. When heated, these seemingly primary inclusions homogenize to a liquid phase in a range between 75°C and 130°C (mean = 100°C) and have final melting temperatures between −0.3° and 0.0°C. The original distribution of Th was broadened during measurements because of fluid inclusion reequilibration. The narrow range of Th in these fluid inclusions suggest unusually consistent V-L ratios. They occur with small, obscure, single phase liquid-filled inclusions, which infer a low temperature origin (less than 60°C), and contradict the higher temperature origin implied by the two phase inclusions.
The diagenetic environment producing these seemingly primary fluid inclusions can be inferred from the origin of the host calcite enclosing them. The δ18O composition of these cements (−4 to−5.5%., PDB) and the fresh water in the fluid inclusions are consistent with precipitation from low-temperature meteoric water. The carbon-isotope composition of the vadose cements that contain only rare two-phase fluid inclusions are comparable to the host rock matrix (δ13C between 0 and +4%., PDB). Cements that contain common two-phase fluid-inclusions have a distinctly lighter carbon isotopic composition of −3 to −5%.. The carbon isotope composition of cements that contain common two-phase inclusions are about 6%. lighter than those of other vadose cements; models of early meteoric diagenesis indicate that this is the result of precipitation from water that has been influenced by soil gas CO2.
Our hypothesis is that the primary fluid inclusions, those with consistent V-L ratios and the single-phase liquid inclusions, form at near-surface temperature (25°C) and pressure when consistent proportions of soil gas and meteoric water percolating through the vadose zone are trapped within elongate vacuoles.
This study corroborates that Th measurements on two phase inclusions in vadose cements can be misleading evidence of thermal diagenesis, even if the measurements are well grouped.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(88)90256-6","issn":"00167037","usgsCitation":"Barker, C., and Halley, R.B., 1988, Fluid inclusions in vadose cement with consistent vapor to liquid ratios, Pleistocene Miami Limestone, southeastern Florida: Geochimica et Cosmochimica Acta, v. 52, no. 5, p. 1019-1025, https://doi.org/10.1016/0016-7037(88)90256-6.","productDescription":"7 p.","startPage":"1019","endPage":"1025","numberOfPages":"7","costCenters":[],"links":[{"id":220668,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"52","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a1277e4b0c8380cd542fc","contributors":{"authors":[{"text":"Barker, C.E.","contributorId":69991,"corporation":false,"usgs":true,"family":"Barker","given":"C.E.","affiliations":[],"preferred":false,"id":366918,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Halley, R. B.","contributorId":87941,"corporation":false,"usgs":true,"family":"Halley","given":"R.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":366919,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70013213,"text":"70013213 - 1988 - Petrology of ultramafic xenoliths from Loihi Seamount, Hawaii","interactions":[],"lastModifiedDate":"2024-06-04T21:14:11.879519","indexId":"70013213","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2420,"text":"Journal of Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Petrology of ultramafic xenoliths from Loihi Seamount, Hawaii","docAbstract":"Ultramafic xenoliths were recovered in four alkalic lava flows from Loihi Seamount at depths between 2200 and 1400m. No xenolith bearing flows were sampled near the summit despite a concentrated dredge program. The flows, three of alkalic basalt and one of basanite, contain common olivine megacrysts and small xenoliths of dunite, rarer harzburgite, and a single wehrlite. Olivine megacrysts as large as 8 mm are Fo84–88 6 and contain magnesiochromite inclusions with 1·1–3·5 wt.% TiO2 Dunite contains Fo83 5–88·5 olivine, magnesiochromite with l·5–6·9 wt.% TiO2 (avg. 3·2 wt.%), and extremely rare chrome-rich diopside. The wehrlite contains euhedral Fo85 9 olivine and magnesiochromite with 1·9–4·7 wt.% TiO2 poikilitically enclosed in chrome-rich diopside (Wo45 4En48 0Fs6·6).Most of the olivine megacrysts, dunite, and the wehrlite are cumulates of Loihi alkalic lavas that accumulated in a magma storage zone located at least 16km below sea level. The rarity of dunite related to tholeiitic magmas supports the interpretation that the alkalic lavas at Loihi generally predate the tholeiitic lavas. The harzburgite xenoliths have cataclastic textures and contain Fo89 5–92 6 olivine, enstatite (Wo2 0–2·7En90·0–88 7Fe8·0–8·6), Cr-rich endiopside (Wo43 4–44 5En52 0–50 0Fs4 6–4 5), and translucent red-brown magnesiochromite. The harzburgite xenoliths, which have 2-pyroxene temperatures of 1066 ± 35°C, originated in the uppermost mantle in a region of high strain rate, probably near the boundary between the mantle and the overlying ocean crust. The presence of upper mantle xenoliths indicates that the magma storage zone is located below the base of the ocean crust within the uppermost mantle.
","language":"English","publisher":"Oxford Academic","doi":"10.1093/petrology/29.6.1161","issn":"00223530","usgsCitation":"Clague, D., 1988, Petrology of ultramafic xenoliths from Loihi Seamount, Hawaii: Journal of Petrology, v. 29, no. 6, p. 1161-1186, https://doi.org/10.1093/petrology/29.6.1161.","productDescription":"26 p.","startPage":"1161","endPage":"1186","numberOfPages":"26","costCenters":[],"links":[{"id":219968,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"29","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a7856e4b0c8380cd78692","contributors":{"authors":[{"text":"Clague, D.A.","contributorId":36129,"corporation":false,"usgs":true,"family":"Clague","given":"D.A.","email":"","affiliations":[],"preferred":false,"id":365557,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70013826,"text":"70013826 - 1988 - Near-bottom currents over the continental slope in the Mid-Atlantic Bight","interactions":[],"lastModifiedDate":"2023-11-30T00:48:29.019181","indexId":"70013826","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1333,"text":"Continental Shelf Research","active":true,"publicationSubtype":{"id":10}},"title":"Near-bottom currents over the continental slope in the Mid-Atlantic Bight","docAbstract":"From a set of 28 current meter records we have found that near-bottom currents faster than 0.2 m s-1 occur frequently over the outer continental shelf of the Mid-Atlantic Bight (bottom depth <210 m) but very rarely (<1% of the time) between bottom depths of 500 m and 2 km over the slope. The rarity of strong near-bottom flow over the middle and lower slope allows the accumulation of fine-grained sediment and organic carbon in this region. Fast near-bottom currents which do occur over the slope are invariably associated with topographic waves, although it is often superimposed inertial oscillations which increase current speed above the level of 0.2 m s-1. Episodes of intense inertial oscillations occur randomly and last typically for 10-20 days. Their energy source is unknown. Topographic wave energy exhibits a slight, but statistically significant, minimum over the mid-slope. These waves appear irregularly and vary both along isobaths and in time. The irregularity is presumably a consequence of random topographic wave generation by Gulf Stream instability. The current regime within sea-floor depressions in the slope (canyons and gullies) is distinctly different from that of the open slope; most notable is the near absence of topographic wave motion within depressions.
","language":"English","publisher":"Elsevier","doi":"10.1016/0278-4343(88)90070-2","issn":"02784343","usgsCitation":"Csanady, G., Churchill, J., and Butman, B., 1988, Near-bottom currents over the continental slope in the Mid-Atlantic Bight: Continental Shelf Research, v. 8, no. 5-7, p. 653-671, https://doi.org/10.1016/0278-4343(88)90070-2.","productDescription":"19 p.","startPage":"653","endPage":"671","numberOfPages":"19","costCenters":[],"links":[{"id":220000,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"8","issue":"5-7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a63d9e4b0c8380cd72728","contributors":{"authors":[{"text":"Csanady, G.T.","contributorId":62340,"corporation":false,"usgs":true,"family":"Csanady","given":"G.T.","email":"","affiliations":[],"preferred":false,"id":366952,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Churchill, J.H.","contributorId":46687,"corporation":false,"usgs":true,"family":"Churchill","given":"J.H.","email":"","affiliations":[],"preferred":false,"id":366951,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Butman, B.","contributorId":85580,"corporation":false,"usgs":true,"family":"Butman","given":"B.","email":"","affiliations":[],"preferred":false,"id":366953,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70014797,"text":"70014797 - 1988 - Ferromanganese deposits from the Gulf of Alaska Seamount Province: Mineralogy, chemistry, and origin","interactions":[],"lastModifiedDate":"2023-09-21T18:41:22.909102","indexId":"70014797","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1168,"text":"Canadian Journal of Earth Sciences","active":true,"publicationSubtype":{"id":10}},"title":"Ferromanganese deposits from the Gulf of Alaska Seamount Province: Mineralogy, chemistry, and origin","docAbstract":"Ferromanganese-oxide deposits dredged from four seamounts (Welker, Miller, Murray, and Patton) in the Gulf of Alaska Seamount Province include poorly crystallized microlaminated crusts on basalt substrate, well-crystallized Mn-oxide veins in epiclastic sedimentary rocks, and crystalline Mn-oxide layers and micronodules in phosphorite. The principal rock types dredged are alkali-basalt pillow fragments and tuffaceous conglomerate and sandstone. The glassy rims of pillow fragments, the glassy goundmass of large volcanic clasts, and the tuffaceous component of the sediment are altered to palagonite. Other low-temperature alteration products include phillipsite, smectite, and carbonate-apatite.Thick (10–50 mm) Fe–Mn crusts consist mainly of δ-MnO2; straight and cuspate growth laminae indicate variable growth rates and periods of nondeposition. A larger number of detrital particles toward the top of thick crusts record the increasing influence of active volcanoes of the Aleutian arc during northwestward movement of the Pacific plate. Thick crusts on basalt substrate have higher Mn/Fe ratios and lower Co content than Fe–Mn crusts from low-latitude seamounts of the central Pacific region. Thin (< 10 mm) crusts on volcaniclastic substrate contain todorokite and birnessite and have higher Mn/Fe ratios, Ni, and Cu and lower Fe and Co than thick Gulf of Alaska crusts.Veins of todorokite and cryptomelane with complex internal structure occur in altered tuffaceous sandstone and conglomerate from Miller Seamount. Fibrous todorokite has a composition similar to those of other marine examples but may contain up to 7% Mn2+ in M2 sites. Microprobe analysis of the marine cryptomelane indicates a composition that is approximately (K,Ba)1–2(Mn4+,Co)7–8O16∙x(H2O).A third type of Fe–Mn deposit in phosphorite is an intimate mixture of todorokite (and minor δ-MnO2)-bearing layers and micronodules, carbonate-apatite, and phillipsite that encloses grains of altered volcanic glass and lithic fragments.The microlaminated structure, mineralogy (predominantly δ-MnO2), and composition (Mn/Fe ratio and transition metal, rare earth element, U, and Th contents) of the thick crusts are characteristic of hydrogenetic Fe–Mn crusts elsewhere in the Pacific. Conversely, the crystallinity and chemical composition of the Mn-oxide veins and thin crusts indicate formation during diagenesis of the volcanogenic sediment substrate. Mn and other transition metals are mobilized during low-temperature oxidative alteration (palagonitization) of basaltic volcanic glass; the oxidation of Fe2+ to Fe3+ during palagonitization and the dissolution of the dilute biogenic fraction of the sediment combine to lower the Eh of ambient pore fluid and enhance the mobility of Mn2+. Diagenesis in the phosphatic sandstone from Patton Seamount involves organic-rich sediment and pore waters elevated in phosphorus owing to upwelling above a large volcanic edifice.
","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/e88-012","issn":"00084077","usgsCitation":"Koski, R., 1988, Ferromanganese deposits from the Gulf of Alaska Seamount Province: Mineralogy, chemistry, and origin: Canadian Journal of Earth Sciences, v. 25, no. 1, p. 116-133, https://doi.org/10.1139/e88-012.","productDescription":"18 p.","startPage":"116","endPage":"133","costCenters":[],"links":[{"id":225914,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Gulf of Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -160.00776514135964,\n 56.04004382192181\n ],\n [\n -159.01538751801613,\n 53.74753893106433\n ],\n [\n -156.60137340653682,\n 51.703580340566106\n ],\n [\n -150.9848921091314,\n 50.173489779545065\n ],\n [\n -143.4294153143174,\n 49.636364635620566\n ],\n [\n -136.0863142147839,\n 49.87286264148247\n ],\n [\n -130.50919580292341,\n 51.75308513520389\n ],\n [\n -131.6945012055195,\n 53.22621260109591\n ],\n [\n -131.38676197343256,\n 53.962297195260106\n ],\n [\n -132.21598643868458,\n 54.99783390695529\n ],\n [\n -133.95067374553372,\n 57.39047623147707\n ],\n [\n -135.86215431332465,\n 58.89865088074984\n ],\n [\n -138.8752696514683,\n 60.005470315111694\n ],\n [\n -140.6687800474778,\n 60.08618247763698\n ],\n [\n -144.04116644543993,\n 60.37646510058818\n ],\n [\n -146.80980626517766,\n 61.2984302351924\n ],\n [\n -149.56871330991953,\n 61.4277042570215\n ],\n [\n -150.339417785037,\n 61.79463577236061\n ],\n [\n -152.29396392062924,\n 61.035036119118644\n ],\n [\n -153.1025371174233,\n 60.095989802565384\n ],\n [\n -154.6801747619648,\n 59.10286769942718\n ],\n [\n -153.94347719022602,\n 58.84839811361036\n ],\n [\n -157.37850426396713,\n 57.231405831475456\n ],\n [\n -160.00776514135964,\n 56.04004382192181\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"25","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0f87e4b0c8380cd53934","contributors":{"authors":[{"text":"Koski, R.A.","contributorId":16006,"corporation":false,"usgs":true,"family":"Koski","given":"R.A.","email":"","affiliations":[],"preferred":false,"id":369322,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70013832,"text":"70013832 - 1988 - The formation and failure of natural dams","interactions":[],"lastModifiedDate":"2023-12-28T00:52:12.021496","indexId":"70013832","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"The formation and failure of natural dams","docAbstract":"Of the numerous kinds of dams that form by natural processes, dams formed from landslides, glacial ice, and late-neoglacial moraines present the greatest threat to people and property. Landslide dams form in a wide range of physiographic settings. The most common types of mass movements that form landslide dams are rock and debris avalanches; rock and soil slumps and slides; and mud, debris, and earth flows. The most common initiation mechanisms for dam-forming landslides are excessive rainfall and snowmelt and earthquakes.
Landslide dams can be classified into six categories based on their relation with the valley floor. Type I dams (11% of 184 landslide dams from around the world that we were able to classify) do not reach from one valley side to the other. Type II dams (44%) span the entire valley floor, in some cases depositing material high on opposite valley sides. Type III dams (41%) move considerable distances both upstream and downstream from the landslide failure. Type IV dams (<1%) are rare and involve the contemporaneous failure of material from both sides of a valley. Type V dams (<1%) also are rare and are created when a single landslide sends multiple tongues of debris into a valley and forms two or more landslide dams in the same reach of river. Type VI dams (3%) involve one or more failure surfaces that extend under the stream or valley and emerge on the opposite valley side.
Many landslide dams fail shortly after formation. In our sample of 73 documented landslide-dam failures, 27% of the landslide dams failed less than 1 day after formation, and about 50% failed within 10 days. Over-topping is by far the most common cause of failure. The timing of failure and the magnitude of the resulting floods are controlled by dam size and geometry; material characteristics of the blockage; rate of inflow to the impoundment; size and depth of the impoundment; bedrock control of flow; and engineering controls such as artificial spill-ways, diversions, tunnels, and planned breaching by blasting or conventional excavation.
Glacial-ice dams can produce at least nine kinds of ice-dammed lakes. The most dangerous are lakes formed in main valleys dammed by tributary glaciers. Failure can occur by erosion of a drainage tunnel under or through the ice dam or by a channel over the ice dam. Cold polar-ice dams generally drain supraglacially or marginally by downmelting of an outlet channel. Warmer, temperate-ice dams tend to fail by sudden englacial or subglacial breaching and drainage.
Late-neoglacial moraine-dammed lakes are located in steep mountain areas affected by the advances and retreats of valley glaciers in the last several centuries. These late-neoglacial dams pose hazards because (1) they are sufficiently young that vegetation has not stabilized their slopes, (2) many dam faces are steeper than the angle of repose, (3) these dams and lakes are immediately downslope from steep crevassed glaciers and near-vertical rock slopes, and (4) downstream from these dams are steep canyons with easily erodible materials that can be incorporated in the flow and increase flood peaks. The most common reported failure mechanism is overtopping and breaching by a wave or series of waves in the lake generated by icefalls, rockfalls, or snow or rock avalanches. Melting of ice cores or frozen ground and piping and seepage are other possible failure mechanisms.
Natural dams may cause upstream flooding as the lake rises and downstream flooding as a result of failure of the dam. Although data are few, for the same potential energy at the dam site, ownstream flood peaks from the failure of glacier-ice dams are smaller than those from landslide, moraine, and structed earth-fill and rock-fill dam failures. Moraine-dam failures appear to produce some of the largest downstream flood peaks for potential energy at the dam site greater than 1011-1012 joules. Differences in flood peaks natural-dam failures appear to be controlled by dam characteristics and failure mechanisms.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1988)100<1054:TFAFON>2.3.CO;2","issn":"00167606","usgsCitation":"Costa, J.E., and Schuster, R.L., 1988, The formation and failure of natural dams: Geological Society of America Bulletin, v. 100, no. 7, p. 1054-1068, https://doi.org/10.1130/0016-7606(1988)100<1054:TFAFON>2.3.CO;2.","productDescription":"15 p.","startPage":"1054","endPage":"1068","numberOfPages":"15","costCenters":[],"links":[{"id":220337,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"100","issue":"7","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0e7de4b0c8380cd534aa","contributors":{"authors":[{"text":"Costa, John E.","contributorId":105743,"corporation":false,"usgs":true,"family":"Costa","given":"John","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":366966,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Schuster, Robert L.","contributorId":19162,"corporation":false,"usgs":true,"family":"Schuster","given":"Robert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":366965,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70014319,"text":"70014319 - 1988 - Garnet compositions and their use as indicators of peraluminous granitoid petrogenesis - southeastern Arabian Shield","interactions":[],"lastModifiedDate":"2012-03-12T17:19:31","indexId":"70014319","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1336,"text":"Contributions to Mineralogy and Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Garnet compositions and their use as indicators of peraluminous granitoid petrogenesis - southeastern Arabian Shield","docAbstract":"Garnet, an uncommon accessory mineral in igneous rocks, occurs in seven small peraluminous granitoid plutons in the southeastern Arabian Shield; textural equilibrium between garnet and other host granitoid minerals indicates that the garnets crystallized from their host magmas. Compositions of the garnets form three groups that reflect host-granitoid compositions, which in turn reflect source compositions and tectonic regimes in which the host magmas were generated. Garnets from the seven plutons have almandine-rich cores and spessartine-rich rims. This reverse zoning depicts host magma compositional evolution; i.e. rimward spessartine enrichment resulted from progressive, host-magma manganese enrichment. The garnets are heavy rare-earth element enriched; (Lu/La)N ranges from 13 to 355 and one of the garnets contains spectacularly elevated abundances of Y, Ta, Th, U, Zn, Zr, Hf, Sn, and Nb. Involvement of garnets with these trace element characteristics in magma genesis or evolution can have dramatic effects on trace element signatures of the resulting magmas. Other researchers suggest that Mn-enriched magmas are most conducive to garnet nucleation. Although the garnetiferous granitoids discussed here are slightly Mn enriched, other genetically similar peraluminous Arabian granitoids lack garnet; Mn enrichment alone does not guarantee garnet nucleation. The presence of excess alumina in the magma may be a prerequisite for garnet nucleation. ?? 1988 Springer-Verlag.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Contributions to Mineralogy and Petrology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Springer-Verlag","doi":"10.1007/BF00373586","issn":"00107999","usgsCitation":"Bray, D., 1988, Garnet compositions and their use as indicators of peraluminous granitoid petrogenesis - southeastern Arabian Shield: Contributions to Mineralogy and Petrology, v. 100, no. 2, p. 205-212, https://doi.org/10.1007/BF00373586.","startPage":"205","endPage":"212","numberOfPages":"8","costCenters":[],"links":[{"id":205628,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00373586"},{"id":225436,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"100","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a14b6e4b0c8380cd54b24","contributors":{"authors":[{"text":"Bray, du","contributorId":28749,"corporation":false,"usgs":true,"family":"Bray","given":"du","email":"","affiliations":[],"preferred":false,"id":368109,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70013795,"text":"70013795 - 1988 - Age and petrology of alkalic postshield and rejuvenated-stage lava from Kauai, Hawaii","interactions":[],"lastModifiedDate":"2012-03-12T17:18:33","indexId":"70013795","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1336,"text":"Contributions to Mineralogy and Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Age and petrology of alkalic postshield and rejuvenated-stage lava from Kauai, Hawaii","docAbstract":"At the top of the Waimea Canyon Basalt on the island of Kauai, rare flows of alkalic postshield-stage hawaiite and mugearite overlie tholeiitic flows of the shield stage. These postshield-stage flows are 3.92 Ma and provide a younger limit for the age of the tholeiitic shield stage. The younger Koloa Volcanics consist of widespread alkalic rejuvenated-stage flows and vents of alkalic basalt, basanite, nephelinite, and nepheline melilitite that erupted between 3.65 and 0.52 Ma. All the flows older than 1.7 Ma occur in the west-northwestern half of the island and all the flows younger than 1.5 Ma occur in the east-southeastern half. The lithologies have no spatial or chronological pattern. The flows of the Koloa Volcanics are near-primary magmas generated by variable small degrees of partial melting of a compositionally heterogeneous garnet-bearing source that has about two-thirds the concentration of P2O5, rare-earth elements, and Sr of the source of the Honolulu Volcanics on the island of Oahu. The same lithology in the Koloa and Honolulu Volcanics is generated by similar degrees of partial melting of distinct source compositions. The lavas of the Koloa Volcanics can be generated by as little as 3 percent to as much as 17 percent partial melting for nepheline melilitite through alkalic basalt, respectively. Phases that remain in the residue of the Honolulu Volcanics, such as rutile and phlogopite, are exhausted during formation of the Koloa Volcanics at all but the smallest degrees of partial melting. The mantle source for Kauai lava becomes systematically more depleted in 87Sr/86Sr as the volcano evolves from the tholeiitic shield stage to the alkalic postshield stage to the alkalic rejuvenated stage: at the same time, the lavas become systematically more enriched in incompatible trace elements. On a shorter timescale, the lavas of the Koloa Volcanics display the same compositional trends, but at a lower rate of change. The source characteristics of the Koloa Volcanics, considered along with those of the Honolulu Volcanics, support a mixing model in which the source of rejuvenated-stage lava represents large-percent melts of a plume source mixed with small amounts of small-percent melts of a heterogeneous mid-ocean-ridge source. ?? 1988 Springer-Verlag.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Contributions to Mineralogy and Petrology","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisherLocation":"Springer-Verlag","doi":"10.1007/BF00371461","issn":"00107999","usgsCitation":"Clague, D., and Dalrymple, G.B., 1988, Age and petrology of alkalic postshield and rejuvenated-stage lava from Kauai, Hawaii: Contributions to Mineralogy and Petrology, v. 99, no. 2, p. 202-218, https://doi.org/10.1007/BF00371461.","startPage":"202","endPage":"218","numberOfPages":"17","costCenters":[],"links":[{"id":205034,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1007/BF00371461"},{"id":220396,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"99","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e8e1e4b0c8380cd47f35","contributors":{"authors":[{"text":"Clague, D.A.","contributorId":36129,"corporation":false,"usgs":true,"family":"Clague","given":"D.A.","email":"","affiliations":[],"preferred":false,"id":366885,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dalrymple, G. B.","contributorId":10407,"corporation":false,"usgs":true,"family":"Dalrymple","given":"G.","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":366884,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70014756,"text":"70014756 - 1988 - Cobalt- and platinum-rich ferromanganese crusts and associated substrate rocks from the Marshall Islands","interactions":[],"lastModifiedDate":"2024-10-15T11:41:39.468786","indexId":"70014756","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Cobalt- and platinum-rich ferromanganese crusts and associated substrate rocks from the Marshall Islands","docAbstract":"To develop a method for quantifying the vegetation of Pennsylvania-age coal beds, of four coal-ball (permineralized peat) profiles and four coal column samples from the Herrin coal bed (Kentucky No. 11) Carbondale Formation in western Kentucky were compared. An estimated 89.5% of the coal can be identified botanically. Compaction ratios for individual tissues were estimated using point counts of organic matter in coal balls. The estimated abundances of major plant groups (lycopods, ferns, sphenopsids, and pteridosperms) in coal balls differ by less than 10% compared to coal after accounting for differential compaction of plant tissues. Standard deviations in taxonomic and maceral composition among coal columns are generally less than 2%.
Consistent differences in botanical composition were found between benches showing that the method is consistent when applied to sufficient thicknesses of coal. It was not possible to make fine-scale correlations within the coal bed using the vegetational data; either the flora varied considerably from place to place or the method of quantification is unreliable for small increments of coal (5 cm or less).
In the coal, pteridosperm abundance is positively correlated with underlying shale partings. This correlation suggests that pteridosperms are favored either by higher nutrient levels or disturbance.
In the third of four benches in the Herrin coal bed, a succession from Sigillaria-containing zones to zones dominated by Lepidophloios hallii is interpreted as a shift towards wetter conditions. In the other benches, the main factors controlling the taxonomic composition appear to have been the relative abundance of nutrients and/or the frequency of disturbance as indicated by the relative abundance of partings.
Criteria for distinguishing between domed and planar swamps are discussed. These include: distribution of partings, type of plant succession, and changes in plant diversity, average plant size, preservational quality and sporinite content. The infrequency of partings in bench C suggests a peat dome developed while the peat of that bench was accumulating but other evidence either fails to support the development of a peat dome or is ambiguous. The maceral composition resembles those of other Carboniferous coals which are thought to have formed from planar peat swamps.
Formation of fusain bands appears to be associated with processes occurring above the peat surface, such as burning or prolonged oxidative exposure. Oxidation of accumulated peat is unlikely because fusain bands rarely include more than a single plant.
Apatite-enriched materials from the Peru shelf have been analyzed for their major oxide and rare earth element (REE) concentrations. The samples consist of (1) the fine fraction of sediment, mostly clay material, (2) phosphatic pellets and fish debris, which are dispersed throughout the fine-grained sediment, (3) tabular-shaped phosphatic crusts, which occur within the uppermost few centimeters of sediment, and (4) phosphatic nodules, which occur on the seafloor. The bulk REE concentrations of the concretions suggest that these elements are partitioned between the enclosed detrital material and the apatite fraction. Analysis of the fine-grained sediment with which the samples are associated suggested that this detrital fraction in the concretions should have shale REE values; the analysis of the fish debris suggested that the apatite fraction might have seawater values. The seawater contribution of REE's is negligible in the nodules and crust, in which the apatite occurs as a fine-grained interstitial cement. That is, the concentration of REE's and the REE patterns are predominantly a function of the amount of enclosed fine-grained sediment. By contrast, the REE pattern of the pelletal apatite suggests a seawater source and the absolute REE concentrations are relatively high. The
A chronosequence of calcic soils formed on granitic glaciofluvial terrace deposits of Rock Creek and the Clarks Fork in south-central Montana shows progressive replacement of aluminosilicate parent-material grains by calcium-magnesium carbonate. The terraces range from late Pliocene to Holocene in age as dated by tephrochronology, correlation, and stream incision rates. Replacement is first seen in soils that are as old as 120,000 yr; the amount and degree of replacement increase in soils older than 120,000 yr along with the development of calcic horizons.
Under the petrographic microscope, carbonate replacement of quartz, feldspars, and the groundmass of andesite grains in Rock Creek soils is shown by embayed grains, networks of carbonate along cracks and between parts of polycrystalline grains and optically aligned grain fragments within carbonate masses. Microprobe data suggest that silica is released by replacement because it is absent from carbonate-filled spaces and is depleted in corrosion pits. Little microscopic evidence exists to support displacement of framework grains by carbonate because fragments of a single grain are rarely rotated out of optical alignment. In the calcic soils of Rock Creek, K-fabric (grains floating in a carbonate matrix) may form by both replacement and displacement.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7061(88)90063-8","usgsCitation":"Reheis, M.C., 1988, Pedogenic replacement of aluminosilicate grains by CaCO3 in Ustollic Haplargids, south-central Montana, U.S.A.: Geoderma, v. 41, no. 3-4, p. 243-261, https://doi.org/10.1016/0016-7061(88)90063-8.","productDescription":"19 p.","startPage":"243","endPage":"261","numberOfPages":"19","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":220493,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.6982421875,\n 44.94924926661153\n ],\n [\n -110.0390625,\n 44.94924926661153\n ],\n [\n -109.2919921875,\n 45.01141864227728\n ],\n [\n -109.2919921875,\n 45.874712248904764\n ],\n [\n -110.6982421875,\n 45.874712248904764\n ],\n [\n -110.6982421875,\n 44.94924926661153\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"41","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a762ce4b0c8380cd77f7e","contributors":{"authors":[{"text":"Reheis, Marith C. 0000-0002-8359-323X mreheis@usgs.gov","orcid":"https://orcid.org/0000-0002-8359-323X","contributorId":138571,"corporation":false,"usgs":true,"family":"Reheis","given":"Marith","email":"mreheis@usgs.gov","middleInitial":"C.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true},{"id":171,"text":"Central Mineral and Environmental Resources Science Center","active":true,"usgs":true}],"preferred":true,"id":366541,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70014351,"text":"70014351 - 1988 - Origin of ultramafic xenoliths containing exsolved pyroxenes from Hualalai Volcano, Hawaii","interactions":[],"lastModifiedDate":"2020-09-26T21:33:28.110339","indexId":"70014351","displayToPublicDate":"1988-01-01T00:00:00","publicationYear":"1988","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1336,"text":"Contributions to Mineralogy and Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Origin of ultramafic xenoliths containing exsolved pyroxenes from Hualalai Volcano, Hawaii","docAbstract":"Hualalai Volcano, Hawaii, is best known for the abundant and varied xenoliths included in the historic 1800 Kaupulehu alkalic basalt flow. Xenoliths, which range in composition from dunite to anorthosite, are concentrated at 915-m elevation in the flow. Rare cumulate ultramafic xenoliths, which include websterite, olivine websterite, wehrlite, and clinopyroxenite, display complex pyroxene exsolution textures that indicate slow cooling. Websterite, olivine websterite, and one wehrlite are spinel-bearing orthopyroxene +olivine cumulates with intercumulus clinopyroxene +plagioclase. Two wehrlite samples and clinopyroxenite are spinel-bearing olivine cumulates with intercumulus clinopyroxene+orthopyroxene + plagioclase. Two-pyroxene geothermometry calculations, based on reconstructed pyroxene compositions, indicate that crystallization temperatures range from 1225° to 1350° C. Migration or unmixing of clinopyroxene and orthopyroxene stopped between 1045° and 1090° C. Comparisons of the abundance of K2O in plagioclase and the abundances of TiO2 and Fe2O3in spinel of xenoliths and mid-ocean ridge basalt, and a single 87Sr/ 86Sr determination, indicate that these Hualalai xenoliths are unrelated to mid-ocean ridge basalt. Similarity between the crystallization sequence of these xenoliths and the experimental crystallization sequence of a Hawaiian olivine tholeiite suggest that the parental magma of the xenoliths is Hualalai tholeiitic basalt. Xenoliths probably crystallized between about 4.5 and 9 kb. The 155°–230° C of cooling which took place over about 120 ka — the age of the youngest Hualalai tholeiitic basalt — yield maximum cooling rates of 1.3×10−3–1.91×10−3 °C/yr. Hualalai ultramafic xenoliths with exsolved pyroxenes crystallized from Hualalai tholeiitic basalt and accumulated in a magma reservoir located between 13 and 28 km below sealevel. We suspect that this reservoir occurs just below the base of the oceanic crust at about 19 km below sealevelz
Over the past 30 years, both isotope geochronology and plate tectonics grew from infancy into authoritative disciplines in the geological sciences. Previously, mountain systems like the Appalachians had been viewed almost entirely in the context of the classical geosyncline, implying a gradualism in stratigraphic and structural change throughout the orogen. Age control, determined largely from distant fossiliferous strata, was unabashedly carried to high-grade metamorphic rocks based only on lithological correlations. With the new concepts in tectonics came the realization that abrupt breaks in stratigraphy and structure occur in many cases at the boundaries of lithotectonic zones. Fortunately, the new techniques of isotope geochronology could be brought to bear directly on the rocks of the immediate study area. This paper chronicles some of the major contributions to the geology of the New England Appalachians that resulted from these efforts during the past three decades.
In tracing the history of geochronologic research, one encounters an increasingly sophisticated approach to the analytical and interpretive aspects of the discipline. Today, the geochronologist can, under optimum conditions, constrain the age of stratigraphic units, igneous activity, deformation, and metamorphism with accuracy that is capable of resolving fine structure within individual orogenic pulses. He participates in full partnership with other colleagues of the science in unravelling the mysteries of mountain building. Several of the topical problems of New England geology in which geochronology played a key role include (1) the recognition and delineation of Avalonia as a Late Proterozoic eastern basement distinct from more western terranes, (2) the dating of the White Mountain Plutonic-Volcanic Suite, a Mesozoic igneous event spanning 100 m.y., and (3) the temporal and spatial separation of structural and metamorphic features imprinted by the Taconic and Acadian orogenies.
The existing geochronology is summarized into a map and table emphasizing the temporal construction of the New England Appalachians. By using lithotectonic zones as the building blocks of the orogen, seven such zones are defined in terms of pre-, syn-, and post-assembly geologic history. From west to east, these lithotectonic zones are (1) Berkshire-Green Mountain, (2) Rowe-Hawley, (3) Connecticut Valley, (4) Bronson Hill, (5) Kearsarge-Central Maine, (6) Tatnic Hill-Nashoba, and (7) Avalonia. Avalonia is further divided into three subzones, Hope Valley, Esmond-Dedham, and Penobscot Bay, which themselves may have had distinct origins and assembly histories. The boundaries between these zones are faults in most cases, some of which may have had recurring movement to further complicate any plate-tectonic scenario.
A delineation of underlying Grenvillian, Chain Lakes, and Avalonian basement is also attempted, which now can make use of isotopes in igneous rocks as petrogenetic indicators to supplement the rare occurrences of basement outcrop within mobile zones of the orogen. The belt of Permian thermal disturbance within the Kearsarge-Central Maine zone is hypothesized to reflect rapid rebound following compressional thickening of underlying Avalonian basement during the Alleghanian orogeny.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1988)100<1168:TDOGSI>2.3.CO;2","usgsCitation":"Zartman, R., 1988, Three decades of geochronologic studies in the New England Appalachians: Geological Society of America Bulletin, v. 100, no. 8, p. 1168-1180, https://doi.org/10.1130/0016-7606(1988)100<1168:TDOGSI>2.3.CO;2.","productDescription":"13 p.","startPage":"1168","endPage":"1180","numberOfPages":"13","costCenters":[],"links":[{"id":225378,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -81.63967460992868,\n 37.399849628117494\n ],\n [\n -69.51076835992886,\n 37.399849628117494\n ],\n [\n -69.51076835992886,\n 45.732269412431236\n ],\n [\n -81.63967460992868,\n 45.732269412431236\n ],\n [\n -81.63967460992868,\n 37.399849628117494\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"100","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb307e4b08c986b325b34","contributors":{"authors":[{"text":"Zartman, R. E.","contributorId":15632,"corporation":false,"usgs":true,"family":"Zartman","given":"R. E.","affiliations":[],"preferred":false,"id":368375,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70162119,"text":"70162119 - 1987 - Testing of male sockeye salmon (Oncorhynchus nerka) and steelhead trout (Salmo gairdneri) for infectious hematopoietic necrosis virus","interactions":[],"lastModifiedDate":"2017-02-12T15:45:42","indexId":"70162119","displayToPublicDate":"2015-10-12T00:00:00","publicationYear":"1987","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1169,"text":"Canadian Journal of Fisheries and Aquatic Sciences","active":true,"publicationSubtype":{"id":10}},"title":" Testing of male sockeye salmon (Oncorhynchus nerka) and steelhead trout (Salmo gairdneri) for infectious hematopoietic necrosis virus","docAbstract":"Infectious hematopoietic necrosis (IHN) virus has been isolated only rarely from whole milt samples of male sockeye salmon (Oncorhynchus nerka). In 3 yr of testing, virus incidences in males ranged from 0 to 13% when milt was sampled but were 60–100% with spleen or kidney. When IHN virus was isolated from sockeye salmon milt at titers less than 3.00 log10 plaque-forming units (pfu)/mL, the level of virus in the kidney or spleen exceeded 7.00 log10 pfu/g. Higher rates of IHN virus isolation from kidney or spleen than from milt were also generally found in steelhead trout (Salmo gairdneri), although the differences were less pronounced than in sockeye salmon. Furthermore, virus was sometimes isolated from steelhead trout milt when the level of virus in kidney or spleen samples was very low, and was recovered from some milt samples when none was isolated from the corresponding spleen sample. When male salmonids are tested for IHN virus, kidney or spleen samples are superior to whole milt, but milt should be included for critical examinations.
","language":"English","publisher":"NRC Research Press","doi":"10.1139/f87-127","usgsCitation":"Mulcahy, D., Pascho, R., and Batts, W., 1987, Testing of male sockeye salmon (Oncorhynchus nerka) and steelhead trout (Salmo gairdneri) for infectious hematopoietic necrosis virus: Canadian Journal of Fisheries and Aquatic Sciences, v. 44, no. 5, p. 1075-1078, https://doi.org/10.1139/f87-127.","productDescription":"4 p.","startPage":"1075","endPage":"1078","costCenters":[{"id":654,"text":"Western Fisheries Research Center","active":true,"usgs":true}],"links":[{"id":314286,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"44","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56978338e4b039675d00a6cc","contributors":{"authors":[{"text":"Mulcahy, D.","contributorId":82642,"corporation":false,"usgs":true,"family":"Mulcahy","given":"D.","email":"","affiliations":[],"preferred":false,"id":588598,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pascho, R.J.","contributorId":65796,"corporation":false,"usgs":true,"family":"Pascho","given":"R.J.","email":"","affiliations":[],"preferred":false,"id":588599,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Batts, W.N. 0000-0002-6469-9004","orcid":"https://orcid.org/0000-0002-6469-9004","contributorId":51043,"corporation":false,"usgs":true,"family":"Batts","given":"W.N.","affiliations":[],"preferred":false,"id":588600,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}