Lake waters of the north‐central U.S.A. are classified into five groups, based on increasing specific conductivity and changes in ionic composition from east to west, from Wisconsin through Minnesota to North and South Dakota. The most dilute group of waters has specific conductivities <29 µmhos · cm−1 at 25°C; the most concentrated group has specific conductances that range from 7,000 to 73,000 µmhos. As conductivity increases all major ions increase, but there is a shift in cation dominance from Ca2 + to Mg2+ to Na+, and in anion dominance from HCO3− to SO42−. This shift partly reflects a westward increase in climatic aridity, and partly a westward sequence of glacial drifts from noncalcareous to calcareous and thence to calcareous with abundant sulfur‐bearing minerals. Levels of pH, K, Cl, F, B, and SiO2 also show a distinct westward increase. Concentrations of NO3− and Mn increase from east to west, but the trend is less distinct. Concentrations of Fe vary widely without any trend over the range of conductivity. Color, mostly from dissolved organic matter, is controlled chiefly by lake depth, except for lakes with extensive peatlands in their drainage basins.
","language":"English","publisher":"Association for the Sciences of Limnology and Oceanography","doi":"10.4319/lo.1983.28.2.0287","usgsCitation":"Gorham, E., Dean, W.E., and Sanger, J., 1983, The chemical composition of lakes in the north‐central United States: Limnology and Oceanography, v. 28, no. 2, p. 287-301, https://doi.org/10.4319/lo.1983.28.2.0287.","productDescription":"15 p.","startPage":"287","endPage":"301","costCenters":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"links":[{"id":480223,"rank":0,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"http://purl.umn.edu/151358","text":"External Repository"},{"id":371120,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Minnesota, North Dakota, South Dakota, Wisconsin","otherGeospatial":"North-central United States","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"MultiPolygon\",\"coordinates\":[[[[-91.217706,43.50055],[-96.591213,43.500514],[-96.439335,43.113916],[-96.630311,42.770885],[-96.483592,42.510345],[-97.302075,42.86566],[-98.035034,42.764205],[-98.568936,42.998537],[-104.053127,43.000585],[-104.048807,48.933636],[-95.153711,48.998903],[-95.153314,49.384358],[-94.878454,49.333193],[-94.640803,48.741171],[-93.818375,48.534442],[-92.984963,48.623731],[-92.634931,48.542873],[-92.698824,48.494892],[-92.341207,48.23248],[-92.066269,48.359602],[-91.542512,48.053268],[-90.88548,48.245784],[-90.703702,48.096009],[-89.489226,48.014528],[-90.735927,47.624343],[-92.058888,46.809938],[-92.025789,46.710839],[-91.781928,46.697604],[-90.880358,46.957661],[-90.78804,46.844886],[-90.920813,46.637432],[-90.327548,46.550262],[-89.929158,46.29975],[-88.141001,45.930608],[-88.13364,45.823128],[-87.831442,45.714938],[-87.887828,45.358122],[-87.647454,45.345232],[-87.72796,45.207956],[-87.59188,45.094689],[-87.983065,44.72073],[-87.970702,44.530292],[-87.021088,45.296541],[-87.73063,43.893862],[-87.910172,43.236634],[-87.800477,42.49192],[-90.614589,42.508053],[-91.078097,42.806526],[-91.177728,43.118733],[-91.062562,43.243165],[-91.217706,43.50055]]],[[[-86.880572,45.331467],[-86.956192,45.351179],[-86.82177,45.427602],[-86.880572,45.331467]]]]},\"properties\":{\"name\":\"Minnesota\",\"nation\":\"USA \"}}]}","volume":"28","issue":"2","noUsgsAuthors":false,"publicationDate":"2003-12-22","publicationStatus":"PW","contributors":{"authors":[{"text":"Gorham, Eville","contributorId":29689,"corporation":false,"usgs":true,"family":"Gorham","given":"Eville","email":"","affiliations":[],"preferred":false,"id":779222,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dean, Walter E. dean@usgs.gov","contributorId":1801,"corporation":false,"usgs":true,"family":"Dean","given":"Walter","email":"dean@usgs.gov","middleInitial":"E.","affiliations":[{"id":318,"text":"Geosciences and Environmental Change Science Center","active":true,"usgs":true}],"preferred":true,"id":779223,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Sanger, J.E.","contributorId":50037,"corporation":false,"usgs":true,"family":"Sanger","given":"J.E.","email":"","affiliations":[],"preferred":false,"id":779224,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70207692,"text":"70207692 - 1983 - Wandering terranes in southern Alaska: The Aleutia Microplate and implications for the Bering Sea","interactions":[],"lastModifiedDate":"2020-06-15T14:48:59.025885","indexId":"70207692","displayToPublicDate":"1983-01-06T14:22:15","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2314,"text":"Journal of Geophysical Research B: Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Wandering terranes in southern Alaska: The Aleutia Microplate and implications for the Bering Sea","docAbstract":"Paleomagnetic and geological data suggest that much of southern Alaska is a collage of tectonostratigraphic terranes which originated in Mesozoic time at paleolatitudes far south of their present position. The time of ‘docking’ of the terranes against cratonic Alaska is critical to defining their amalgamated size and extent during their northward motion as well as their role in the evolution of the Bering Sea. One of the largest of the tectonostratigraphic terranes, the Peninsular terrane of south central and southwestern Alaska, extends offshore along the outer Bering Sea continental margin (Beringia). Paleomagnetic data suggest that this terrane has moved northward through all of Cenozoic time, but geologic data imply that the terrane had accreted to Alaska by the end of the Mesozoic. In early Cenozoic time the eastern part of the Aleutian arc appears to have been superimposed on the Peninsular terrane, and postulated northward Cenozoic motion of the terrane would therefore have required northward motion of the arc. Two accretion models, based on docking times for terranes in Alaska, are proposed, and they illustrate that large areas of the abyssal Bering Sea, the Alaska Peninsula, the Aleutian arc, and the Beringian continental margin may be part of a superterrane or microplate called Aleutia (microplate as defined by Beck et al. (1980), i.e., a microplate is a displaced segment of lithosphere that has crustal roots, whereas a superterrane is an amalgamation of terranes which may or may not be rootless). Model A implies that the Aleutian arc developed in situ on the southern edge of Aleutia after the microplate had docked. In model B, the final docking time of the Peninsular terrane is late Cenozoic, which implies that the Aleutia microplate encompasses a mammoth area that includes parts of southern Alaska, the Alaska Peninsula, the southern Beringian margin, the abyssal Bering Sea (Kula plate), and the Aleutian arc. If model A is correct, the docking time of the Peninsular terrane is late Mesozoic or earliest Tertiary. The Aleutia microplate in this model is made up solely of the abyssal Bering Sea (Kula plate), which presumably docked at the same time or slightly after the Peninsular terrane accreted against Alaska. If model B is correct, that is, if the Aleutia collided with nuclear Alaska during the Cenozoic, then a late Cenozoic suture zone, the vestige of a large open sea that must have closed between Aleutia and Alaska, must exist in south central and southwest Alaska. Either evidence for Cenozoic closure and suturing has been obliterated in Alaska or the inferences of Cenozoic terrane motion derived from paleomagnetic data are suspect.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB088iB04p03439","usgsCitation":"Marlow, M.S., and Cooper, A.K., 1983, Wandering terranes in southern Alaska: The Aleutia Microplate and implications for the Bering Sea: Journal of Geophysical Research B: Solid Earth, v. 88, no. B4, p. 3439-3446, https://doi.org/10.1029/JB088iB04p03439.","productDescription":"8 p.","startPage":"3439","endPage":"3446","costCenters":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":371021,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Southern Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -167.51953124999997,\n 57.70414723434193\n ],\n [\n -173.49609375,\n 57.088515327886505\n ],\n [\n -169.1015625,\n 52.64306343665892\n ],\n [\n -159.2578125,\n 53.4357192066942\n ],\n [\n -155.830078125,\n 56.84897198026975\n ],\n [\n -162.7734375,\n 58.07787626787517\n ],\n [\n -167.51953124999997,\n 57.70414723434193\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"88","issue":"B4","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","contributors":{"authors":[{"text":"Marlow, Michael S.","contributorId":72775,"corporation":false,"usgs":true,"family":"Marlow","given":"Michael","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":778986,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cooper, Alan K. acooper@usgs.gov","contributorId":2854,"corporation":false,"usgs":true,"family":"Cooper","given":"Alan","email":"acooper@usgs.gov","middleInitial":"K.","affiliations":[{"id":520,"text":"Pacific Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":true,"id":778987,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70120417,"text":"70120417 - 1983 - Use of pine nuts by grizzly and black bears in the Yellowstone area","interactions":[],"lastModifiedDate":"2014-08-14T11:39:08","indexId":"70120417","displayToPublicDate":"1983-01-01T11:19:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":978,"text":"Bears: Their Biology and Management","active":true,"publicationSubtype":{"id":10}},"title":"Use of pine nuts by grizzly and black bears in the Yellowstone area","docAbstract":"The large seeds (pine nuts) of whitebark pine are commonly eaten in the spring (March-May) and fall (September-November) by grizzly and black bears in Yellowstone National Park and adjacent areas (Craighead and Craighead 1972, Blanchard 1978, Mealey 1980) and western Montana (Tisch 1961; J. Sumner and J. J. Craighead, unpubl. rep., Montant Coop. Wildl. Res. Unit, Univ. Montana, Missoula, 1973). Similar nuts from limber pine are eaten by grizzly bears on the east Rocky Mountain Front of northwestern Montana (Schallenberger and Jonkel, annual rep., Border Grizzly Project, Univ. Montana, Missoula, 1980). The nuts of the European stone pine (P. cembra) are an important food for brown bears (U. arctos) throughout the taiga zone in the Soviet Union (Pavlov and Zhdanov 1972, Ustinov 1972, Yazan 1972). Both the production of whitebark pine cones (Forcella 1977, Blanchard 1978, Mealey 1980) and the quantity of nuts consumed by bears vary annually (Mealey 1975, Blancard 1978).
\nPine nuts are also an important food for red squirrels in whitebark forests. In fall, squirrels remove cones from trees and cache them in middens. Bears as well as other mammalian and avian seed predators compete with squirrels for whitebark nuts (Forcella 1977, Tomback 1977).
\nConfusion about the ripening process of whitebark pine cones has resulted in errors in the literature on the availability of pine nuts as a bear food. Whitebark cones are indehiscent and do not disintegrate (Tomback 1981). Vertebrate foraging probably leaves few, if any, seed-bearing cones on trees by late fall; the cones remaining abscise sometime thereafter (Tomback 1981). Because cones do not abscise or release their seed in fall, bears may obtain pine nuts in 2 ways. Black bears may climb whitebark pine trees and break off cone-bearing brnahces to feed on cones (Tisch 1961, Mealey 1975, Forcella 1977); or both black bears and grizzly bears may raid squirrel caches to feed on pine nuts (Tisch 1961, Craighead and Craighead 1972, Blanchard 1978). The purpose of this study was to determine (1) the major source of pine nuts for bears, (2) why cone scales do not appear in bear scat containing pine nuts, and (3) what factors influence bear use of pine nuts.
","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Bears: Their Biology and Management","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"International Conference on Bear Research and Management","publisherLocation":"New York, NY","doi":"10.2307/3872534","usgsCitation":"Kendall, K.C., 1983, Use of pine nuts by grizzly and black bears in the Yellowstone area: Bears: Their Biology and Management, v. 5, p. 166-173, https://doi.org/10.2307/3872534.","productDescription":"8 p.","startPage":"166","endPage":"173","numberOfPages":"8","costCenters":[],"links":[{"id":292188,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":292187,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.2307/3872534"}],"country":"United States","otherGeospatial":"Yellowstone National Park","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -111.156,44.1324 ], [ -111.156,45.109 ], [ -109.8242,45.109 ], [ -109.8242,44.1324 ], [ -111.156,44.1324 ] ] ] } } ] }","volume":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53edcd56e4b0f61b386d24be","contributors":{"authors":[{"text":"Kendall, Katherine C. 0000-0002-4831-2287 kkendall@usgs.gov","orcid":"https://orcid.org/0000-0002-4831-2287","contributorId":3081,"corporation":false,"usgs":true,"family":"Kendall","given":"Katherine","email":"kkendall@usgs.gov","middleInitial":"C.","affiliations":[{"id":481,"text":"Northern Rocky Mountain Science Center","active":true,"usgs":true}],"preferred":true,"id":498178,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012067,"text":"70012067 - 1983 - Isotopic evidence from the eastern Canadian shield for geochemical discontinuity in the proterozoic mantle","interactions":[],"lastModifiedDate":"2012-03-12T17:19:03","indexId":"70012067","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Isotopic evidence from the eastern Canadian shield for geochemical discontinuity in the proterozoic mantle","docAbstract":"Most workers agree that Proterozoic anorthosite massifs represent the crystallization products of mantle-derived magmas1,2, although the composition of the parental melts is a major unsolved petrological problem 3. As mantle-derived rocks, the massifs can be used as geochemical probes of their late Precambrian upper mantle sources. We report here Nd and Sr isotopic compositions of anorthosites and related rocks from the Grenville and Nain Provinces of the eastern Canadian shield. Here 75% of the Earth's known anorthosite is found in a 1,600-km belt from the Adirondack Mountains of northern New York State to the eastern coast of Labrador4 (Fig. 1). The results indicate that the massifs were derived from at least two distinct mantle source regions which were established before 1,650 Myr ago, and were episodically involved in magmatism over ???500 Myr. One reservoir, below the Grenville Province, and probably below much of the eastern Superior Province, was isotopically similar to the depleted, modern-day mid-ocean ridge basalt (MORB) source. The other reservoir was chondritic to moderately enriched, and is most easily identified in the Nain Province, but may have occurred scattered throughout the Superior Province. ?? 1983 Nature Publishing Group.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Nature","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1038/306679a0","issn":"00280836","usgsCitation":"Ashwal, L., and Wooden, J.L., 1983, Isotopic evidence from the eastern Canadian shield for geochemical discontinuity in the proterozoic mantle: Nature, v. 306, no. 5944, p. 679-680, https://doi.org/10.1038/306679a0.","startPage":"679","endPage":"680","numberOfPages":"2","costCenters":[],"links":[{"id":222455,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":205241,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1038/306679a0"}],"volume":"306","issue":"5944","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a3fb1e4b0c8380cd64736","contributors":{"authors":[{"text":"Ashwal, L.D.","contributorId":82060,"corporation":false,"usgs":true,"family":"Ashwal","given":"L.D.","email":"","affiliations":[],"preferred":false,"id":362654,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wooden, J. L.","contributorId":58678,"corporation":false,"usgs":true,"family":"Wooden","given":"J.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":362653,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":28089,"text":"wri834053 - 1983 - Ground water in the northeast part of Twentynine Palms Marine Corps Base, Bagdad area, California","interactions":[],"lastModifiedDate":"2023-04-11T19:27:17.935961","indexId":"wri834053","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"83-4053","title":"Ground water in the northeast part of Twentynine Palms Marine Corps Base, Bagdad area, California","docAbstract":"The hydrologic characteristics of the Bagdad area, in the northeast part of Twentynine Palms Marine Corps Base, were investigated to determine the feasibility of obtaining a supply of ground water. Five test holes were drilled and three of these were completed with 6-inch casings. Ground water in the eastern part of the study area is high in dissolved solids; water from well 5N/11E-36H1 contains 252,000 milligrams per liter of dissolved solids, and well 4N/12E-7R1 contains 21,800 milligrams per liter of dissolved solids. The dissolved-solids concentration in water from the test wells on the west side of Ludlow fault is much lower; the dissolved solids in water from the three test wells ranges from 669 to 961 milligrams per liter. The recommended limits for chloride and fluoride were exceeded in water from test well 4N/10E-21K1, arsenic and fluoride in water from well 5N/9E-3B1, and chloride in water from test well 6N/9E-34F1. An estimated 640,000 acre-feet of water is stored in the alluvium west of the Ludlow fault, sufficient to provide for several small diameter wells for many years.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wri834053","usgsCitation":"Koehler, J.H., 1983, Ground water in the northeast part of Twentynine Palms Marine Corps Base, Bagdad area, California: U.S. Geological Survey Water-Resources Investigations Report 83-4053, iv, 15 p., https://doi.org/10.3133/wri834053.","productDescription":"iv, 15 p.","costCenters":[],"links":[{"id":415591,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_35692.htm","linkFileType":{"id":5,"text":"html"}},{"id":56908,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1983/4053/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":123623,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1983/4053/report-thumb.jpg"}],"country":"United States","state":"Calilfornia","otherGeospatial":"Twentynine Palms Marine Corps Base","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.74714785522053,\n 34.772980861725955\n ],\n [\n -116.74714785522053,\n 34.196058657436936\n ],\n [\n -115.70337642189573,\n 34.196058657436936\n ],\n [\n -115.70337642189573,\n 34.772980861725955\n ],\n [\n -116.74714785522053,\n 34.772980861725955\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ab0e4b07f02db66d7b2","contributors":{"authors":[{"text":"Koehler, J. H.","contributorId":108108,"corporation":false,"usgs":true,"family":"Koehler","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":199198,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011383,"text":"70011383 - 1983 - The compositionally zoned eruption of 1912 in the Valley of Ten Thousand Smokes, Katmai National Park, Alaska","interactions":[],"lastModifiedDate":"2020-10-03T15:51:38.932929","indexId":"70011383","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"The compositionally zoned eruption of 1912 in the Valley of Ten Thousand Smokes, Katmai National Park, Alaska","docAbstract":"On June 6–8, 1912, ∼ 15 km3 of magma erupted from the Novarupta caldera at the head of the Valley of Ten Thousand Smokes (VTTS), producing ∼ 20 km3 of air-fall tephra and 11–15 km3 of ash-flow tuff within ∼ 60 hours. Three discrete periods of ash-fall at Kodiak correlate, respectively, with Plinian tephra layers designated A, CD, and FG by Curtis (1968) in the VTTS. The ash-flow sequence overlapped with but outlasted pumice fall A, terminating within 20 hours of the initial outbreak and prior to pumice fall C. Layers E and H consist mostly of vitric dust that settled during lulls, and Layer B is the feather edge of the ash flow. The fall units filled and obscured the caldera, but arcuate and radial fissures outline a 6-km2 depression. The Novarupta lava dome and its ejecta ring were emplaced later within the depression. At Mt. Katmai, 10 km east of the 1912 vent, a 600-m-deep caldera of similar area also collapsed at about this time, probably owing to hydraulic connection with the venting magma system; but all known ejecta are thought to have erupted at Novarupta. Mingling of three distinctive magmas during the eruption produced an abundance of banded pumice, and mechanical mixing of chilled ejecta resulted in deposits with a wide range of bulk composition. Pumice in the initial fall unit (A) is 100% rhyolite, but fall units atop the ash flow are > 98% dacite; black andesitic scoria is common only in the ash flows and in near-vent air-fall tephra. Pumice counts show the first half of the ash-flow deposit to be 91–98% rhyolite, but progressive increases of dacite and andesite eventually reduced the rhyolitic component to < 2%. The later, rhyolite-poor flows were hotter, less mobile, and widely produced partially welded tuff and vapor-indurated sillar.
The main ash flow was too deflated and sluggish 16 km from the vent to surmount a 25-m-high moraine in its path but was diverted around it and continued 5 km down-valley, engulfing and charring trees but not toppling all of them. Thin ash-flow veneers feather 30–40 m up the enclosing valley walls but only where a constriction in the central VTTS locally raised the flow level. In the upper VTTS, the “high sand mark” is not a veneer but a marginal bench formed in thick tuff by differential compaction. Flooding from adjacent glaciers led to phreatic explosions that ejected blocks of tuff more welded than any yet exposed. A cluster of phreatic craters dammed a lake atop the tuff, the breaching of which caused a flood that scoured the ash-flow surface in the central VTTS, transported 50-cm blocks of welded tuff > 20 km to the lowermost VTTS, and deposited 1–8 m of debris there.
Rhyolitic ejecta contain only 1–2% phenocrysts but andesite and dacite have 30–45%. Quartz is present and augite absent only in the rhyolite, but all ejecta contain plagioclase, orthopyroxene, titanomagnetite, ilmenite, apatite, and pyrrhotite; rare olivine occurs in the andesite. The zoning ranges of phenocrysts in the rhyolitic and intermediate ejecta do not overlap. New chemical data show the bulk SiO2 range to be: rhyolite 77 ± 0.6, dacite 66-64.5, and andesite 61.5–58.5%. The dacitic and andesitic ejecta contrast in color and density, and it is not certain whether they form a compositional continuum. Analyses reported by Fenner within the 66–76% SiO2 range were of banded pumice and lava and of bulk tephra that mechanically fractionated and mixed during flight. Despite the gap of 10% SiO2, Fe-Ti-oxide temperatures show a continuous range from rhyolite (805–850°C) through dacite (855–955°C) to andesite (955–990°C). Thermal continuity and isotopic and trace-element data suggest that all were derived from a single magmatic system, whether or not they were physically contiguous before eruption. If the rhyolitic liquid separated from dacitic magma, extraction was so efficient that no dacitic phenocrysts were retained and no bulk compositions in the range 66–76% SiO2 were created; if it were a partial melt of roof rocks atop an intermediate magma body, then such rocks had no O- or Sr-isotopic contrast with the andesite-dacite magma and clearly did not include the Jurassic arkosic or granitic basement. The presence of Holocene domes of pre-1912 glassy dacite adjacent to the 1912 vent suggest that the 7 km3 (or more) of high-silica rhyolitic magma (a composition rare in the Aleutian arc) was generated in less than a few thousand years. The 1912 vent is semi-encircled by several andesitic stratocones and is as close to Mageik, Trident, and Griggs volcanoes as it is to Mt. Katmai. The erupted magma probably occupied only shallow levels of an extensive system of injection and storage under a cluster of several stratovolcanoes. Although Quaternary basalt is not known to have erupted here, the intrusion of basaltic magma probably sustains the greater-VTTS magmatic system.
","language":"English","publisher":"Elsevier","doi":"10.1016/0377-0273(83)90003-3","issn":"03770273","usgsCitation":"Hildreth, W., 1983, The compositionally zoned eruption of 1912 in the Valley of Ten Thousand Smokes, Katmai National Park, Alaska: Journal of Volcanology and Geothermal Research, v. 18, no. 1-4, p. 1-56, https://doi.org/10.1016/0377-0273(83)90003-3.","productDescription":"56 p.","startPage":"1","endPage":"56","numberOfPages":"56","costCenters":[],"links":[{"id":221521,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Katmai National Park","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -156.368408203125,\n 57.66303463288711\n ],\n [\n -153.25927734375,\n 57.66303463288711\n ],\n [\n -153.25927734375,\n 59.33318942659219\n ],\n [\n -156.368408203125,\n 59.33318942659219\n ],\n [\n -156.368408203125,\n 57.66303463288711\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"18","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505baa4ee4b08c986b3227c4","contributors":{"authors":[{"text":"Hildreth, W. 0000-0002-7925-4251","orcid":"https://orcid.org/0000-0002-7925-4251","contributorId":100487,"corporation":false,"usgs":true,"family":"Hildreth","given":"W.","affiliations":[],"preferred":false,"id":360971,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70012100,"text":"70012100 - 1983 - Eastern Devonian shales: Organic geochemical studies, past and present","interactions":[],"lastModifiedDate":"2012-03-12T17:19:06","indexId":"70012100","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Eastern Devonian shales: Organic geochemical studies, past and present","docAbstract":"The Eastern Devonian shales are represented by a sequence of sediments extending from New York state, south to the northern regions of Georgia and Alabama, and west into Ohio and to the Michigan and Ilinois Basins. Correlatives are known in Texas. The shale is regionally known by a number of names: Chattanooga, Dunkirk, Rhinestreet, Huron, Antrim, Ohio, Woodford, etc. These shales, other than those in Texas, have elicited much interest because they have been a source of unassociated natural gas. It is of particular interest, however, that most of these shales have no associated crude oil, in spite of the fact that they have some of the characteristics normally attributed to source beds. This paper addresses some of the organic geochemical aspects of the kerogen in these shales, in relation to their oil generating potential. Past organic geochemical studies on Eastern Devonian shales will be reviewed. Recent solid state 13C NMR studies on the nature of the organic matter in Eastern Devonian shales show that Eastern Devonian shales contain a larger fraction of aromatic carbon in their chemical composition. Thus, despite their high organic matter contents, their potential as a petroleum source rock is low, because the kerogen in these shales is of a \"coaly\" nature and hence more prone to producing natural gas.","largerWorkTitle":"Preprints Symposia","language":"English","issn":"05693799","usgsCitation":"Breger, I.A., Hatcher, P.G., Romankiw, L., and Miknis, F., 1983, Eastern Devonian shales: Organic geochemical studies, past and present, in Preprints Symposia, v. 28, no. 1.","startPage":"73","costCenters":[],"links":[{"id":221803,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"28","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0532e4b0c8380cd50cd0","contributors":{"authors":[{"text":"Breger, Irving A.","contributorId":65205,"corporation":false,"usgs":true,"family":"Breger","given":"Irving","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":362730,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hatcher, Patrick G.","contributorId":93625,"corporation":false,"usgs":true,"family":"Hatcher","given":"Patrick","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":362732,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Romankiw, L.A.","contributorId":85724,"corporation":false,"usgs":true,"family":"Romankiw","given":"L.A.","affiliations":[],"preferred":false,"id":362731,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Miknis, F.P.","contributorId":61564,"corporation":false,"usgs":true,"family":"Miknis","given":"F.P.","email":"","affiliations":[],"preferred":false,"id":362729,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70011241,"text":"70011241 - 1983 - LITHOLOGIC MAPPING USING LANDSAT THEMATIC MAPPER DATA.","interactions":[],"lastModifiedDate":"2012-03-12T17:18:28","indexId":"70011241","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"LITHOLOGIC MAPPING USING LANDSAT THEMATIC MAPPER DATA.","docAbstract":"The paper is in abstract form. It discusses the Landsat-4 Thematic Mapper (TM), with its new near infrared bands centered at 1. 65 mu m and 2. 20 mu m and spatial resolution of 30 m, which has been used to distinguish rocks containing minerals having ferric-iron absorption bands in the visible and near-infrared and Al-O and CO//3 absorption bands in the 2. 1-2. 4 mu m regions. On the basis of characteristic absorption bands, digitally processed TM data were used to differentiate vegetated from non-vegetated areas, limonitic from nonlimonitic rocks, rocks containing minerals having absorption bands in the near-infrared region from rocks lacking the infrared absorption bands. Specific minerals were detected in both the humid eastern and semi-arid western United States. The absorption bands in the near-infrared region were used to detect kaolinite in open-pit exposures of a kaolin mining district near Macon, Georgia; calcium carbonate in the beach sands along the east coast of Florida; and kaolinite, alunite, jarosite, sericite and gypsum in natural exposures near Boulder City, Nevada.","conferenceTitle":"Proceedings - Pecora VIII Symposium: Satellite Land Remote Sensing Advancements for the Eighties.","conferenceLocation":"Sioux Falls, ND, USA","language":"English","publisher":"Augustana Coll","publisherLocation":"Sioux Falls, SD, USA","usgsCitation":"Podwysocki, M.H., Salisbury, J., Jones, O.D., and Mimms, D., 1983, LITHOLOGIC MAPPING USING LANDSAT THEMATIC MAPPER DATA., Proceedings - Pecora VIII Symposium: Satellite Land Remote Sensing Advancements for the Eighties., Sioux Falls, ND, USA.","startPage":"169","costCenters":[],"links":[{"id":221432,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a40e9e4b0c8380cd65136","contributors":{"authors":[{"text":"Podwysocki, M. H.","contributorId":70391,"corporation":false,"usgs":true,"family":"Podwysocki","given":"M.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":360644,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Salisbury, J.W.","contributorId":78352,"corporation":false,"usgs":true,"family":"Salisbury","given":"J.W.","email":"","affiliations":[],"preferred":false,"id":360645,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jones, O. D.","contributorId":42700,"corporation":false,"usgs":true,"family":"Jones","given":"O.","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":360643,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mimms, D.L.","contributorId":39522,"corporation":false,"usgs":true,"family":"Mimms","given":"D.L.","email":"","affiliations":[],"preferred":false,"id":360642,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":3192,"text":"wsp2195 - 1983 - Hydrology of the Ferron Sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah, with a section on stratigraphy and a section on leaching of overburden","interactions":[{"subject":{"id":23739,"text":"ofr81535 - 1981 - Hydrology of the Ferron sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah","indexId":"ofr81535","publicationYear":"1981","noYear":false,"title":"Hydrology of the Ferron sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah"},"predicate":"SUPERSEDED_BY","object":{"id":3192,"text":"wsp2195 - 1983 - Hydrology of the Ferron Sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah, with a section on stratigraphy and a section on leaching of overburden","indexId":"wsp2195","publicationYear":"1983","noYear":false,"title":"Hydrology of the Ferron Sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah, with a section on stratigraphy and a section on leaching of overburden"},"id":1}],"lastModifiedDate":"2023-11-29T22:45:01.092093","indexId":"wsp2195","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"2195","title":"Hydrology of the Ferron Sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah, with a section on stratigraphy and a section on leaching of overburden","docAbstract":"Coal in the Ferron Sandstone Member of the Mancos Shale of Cretaceous age has traditionally been mined by underground techniques in the Emery Coal Field in the southern end of Castle Valley in east-central Utah. However, approximately 99 million tons are recoverable by surface mining. Ground water in the Ferron is the sole source of supply for the town of Emery, but the aquifer is essentially untapped outside the Emery area.
The Ferron Sandstone Member crops out along the eastern edge of Castle Valley and generally dips 2 ? to 10 ? to the northwest. Sandstones in the Ferron are enclosed between relatively impermeable shale in the Tununk and Blue Gate Members of the Mancos Shale. Along the outcrop, the Ferron ranges in thickness from about 80 feet in the northern part of Castle Valley to 850 feet in the southern part. The Ferron also generally thickens in the subsurface downdip from the outcrop. Records from wells and test holes indicate that the full thickness of the Ferron is saturated with water in most areas downdip from the outcrop area.
Tests in the Emery area indicate that transmissivity of the Ferron sandstone aquifer ranges from about 200 to 700 feet squared per day where the Ferron is fully saturated. Aquifer transmissivity is greatest near the Paradise Valley-Joes Valley fault system where permeability has been increased by fracturing. Storage coefficient ranges from about 10 .6 to 10 -3 where the Ferron sandstone aquifer is confined and probably averages 5 x 10-2 where it is unconfined.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp2195","collaboration":"Prepared in cooperation with the United States Bureau of Land Management","usgsCitation":"Lines, G.C., Morrissey, D.J., Ryer, T.A., and Fuller, R.H., 1983, Hydrology of the Ferron Sandstone aquifer and effects of proposed surface-coal mining in Castle Valley, Utah, with a section on stratigraphy and a section on leaching of overburden: U.S. Geological Survey Water Supply Paper 2195, Report: vi, 40 p.; 3 Plates: 17.00 x 27.20 inches, https://doi.org/10.3133/wsp2195.","productDescription":"Report: vi, 40 p.; 3 Plates: 17.00 x 27.20 inches","numberOfPages":"46","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":30174,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2195/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing location of selected wells, springs, and test holes in and near Castle Valley, Utah, where ground-water information is available, 1980"},{"id":30175,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2195/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing the thickness of the Ferron sandstone member of the Mancos shale in Castle Valley, Utah"},{"id":423046,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25538.htm","linkFileType":{"id":5,"text":"html"}},{"id":138109,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/2195/report-thumb.jpg"},{"id":30177,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/2195/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":30176,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/2195/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing the altitude of the top of the Ferron Sandstone member of the Mancos Shale in Castle Valley, Utah"}],"country":"United States","state":"Utah","otherGeospatial":"Castle Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -110.5,\n 39.75\n ],\n [\n -111.5,\n 39.75\n ],\n [\n -111.5,\n 38.5\n ],\n [\n -110.5,\n 38.5\n ],\n [\n -110.5,\n 39.75\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aa7e4b07f02db667150","contributors":{"authors":[{"text":"Lines, Gregory C.","contributorId":50502,"corporation":false,"usgs":true,"family":"Lines","given":"Gregory","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":146406,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Morrissey, Daniel J.","contributorId":89875,"corporation":false,"usgs":true,"family":"Morrissey","given":"Daniel","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":146408,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ryer, Thomas A.","contributorId":100359,"corporation":false,"usgs":true,"family":"Ryer","given":"Thomas","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":146409,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Fuller, Richard H.","contributorId":66236,"corporation":false,"usgs":true,"family":"Fuller","given":"Richard","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":146407,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70011600,"text":"70011600 - 1983 - The saltwater-freshwater interface in the Tertiary limestone aquifer, southeast Atlantic outer-continental shelf of the U.S.A.","interactions":[],"lastModifiedDate":"2025-04-11T16:49:26.1536","indexId":"70011600","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2342,"text":"Journal of Hydrology","active":true,"publicationSubtype":{"id":10}},"title":"The saltwater-freshwater interface in the Tertiary limestone aquifer, southeast Atlantic outer-continental shelf of the U.S.A.","docAbstract":"Hydrologic testing in an offshore oil well abandoned by Tenneco, Inc., determined the position of the saltwater-freshwater interface in Tertiary limestones underlying the Florida-Georgia continental shelf of the U.S.A. Previous drilling (JOIDES and U.S.G.S. AMCOR projects) established the existence of freshwater far offshore in this area. At the Tenneco well 55 mi. (∼88 km) east of Fernandina Beach, Florida, drill-stem tests made in the interval 1050–1070 ft. (320–326 m) below sea level in the Ocala Limestone recovered a sample with a chloride concentration of 7000 mg l−1. Formation water probably is slightly fresher. Pressure-head measurements indicated equivalent freshwater heads of 24–29 ft. (7.3–8.8 m) above sea level.
At the coast (Fernandina Beach), a relatively thin transition zone separating freshwater and saltwater occurs at a depth of 2100 ft. (640 m) below sea level. Fifty-five miles (∼88 km) offshore, at the Tenneco well, the base of freshwater is ∼1100 ft. (∼335 m) below sea level. The difference in approximate depth to the freshwater-saltwater transition at these two locations suggests an interface with a very slight landward slope. Assuming the Hubbert interface equation applies here (because the interface and therefore freshwater flow lines are nearly horizontal) the equilibrium depth to the interface should be 40 times the freshwater head above sea level. Using present-day freshwater heads along the coast in the Hubbert equation results in depths to the interface of less than the observed 2100 ft. (640 m). Substituting predevelopment heads in the equation yields depths greater than 2100 ft. (640 m). Thus the interface appears to be in a transient position between the position that would be compatible with present-day heads and the position that would be compatible with predevelopment heads. This implies that some movement of the interface from the predevelopment position has occurred during the past hundred years. The implied movement is incompatible with the hypothesis that the freshwater occurring far offshore in this area is trapped water remaining since the Pleistocene Epoch.
","language":"English","publisher":"Elsevier","doi":"10.1016/0022-1694(83)90251-2","issn":"00221694","usgsCitation":"Johnston, R., 1983, The saltwater-freshwater interface in the Tertiary limestone aquifer, southeast Atlantic outer-continental shelf of the U.S.A.: Journal of Hydrology, v. 61, no. 1-3, p. 239-249, https://doi.org/10.1016/0022-1694(83)90251-2.","productDescription":"11 p.","startPage":"239","endPage":"249","costCenters":[],"links":[{"id":220712,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida, Georgia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -82.49895094186574,\n 30.906206797439737\n ],\n [\n -82.49895094186574,\n 29.80296540535703\n ],\n [\n -81.27672743461723,\n 29.80296540535703\n ],\n [\n -81.27672743461723,\n 30.906206797439737\n ],\n [\n -82.49895094186574,\n 30.906206797439737\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"61","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bafb0e4b08c986b324998","contributors":{"authors":[{"text":"Johnston, R.H.","contributorId":19536,"corporation":false,"usgs":true,"family":"Johnston","given":"R.H.","email":"","affiliations":[],"preferred":false,"id":361516,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":44504,"text":"wri834045 - 1983 - Hydrogeologic and water-quality characteristics of the Prairie du Chien-Jordan aquifer, Southeast Minnesota","interactions":[],"lastModifiedDate":"2023-03-13T21:29:01.182397","indexId":"wri834045","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"83-4045","title":"Hydrogeologic and water-quality characteristics of the Prairie du Chien-Jordan aquifer, Southeast Minnesota","docAbstract":"Quality of water in the Prairie du Chien-Jordan aquifer is generally good, except for some localized contamination, Coal-tar derivatives that contaminate the aquifer in St. Louis Park, a western suburb in the Twin Cities Metropolitan Area, pose the most serious threat to water quality. High hardness and iron concentration limit suitability for municipal and industrial use in parts of extreme southeast Minnesota. Confining beds of bedrock and drift, however, protect most of the aquifer from surface pollutants.
The Prairie du Chien-Jordan aquifer is part of a sequence of sedimentary bedrock units in southeast Minnesota. The Jordan Sandstone is a white to yellow, fine- to coarse-grained sandstone. The Prairie du Chien Group comprises two dolomitic formations that are vuggy and fractured and interbedded with thin layers of shale. The aquifer formations were deposited in Paleozoic seas that occupied the Hollandale embayment. The aquifer dips toward the interior of the embayment where it is as deep as 750 feet below land surface and as thick as 500 feet.
Permeability is secondary in the Prairie du Chien Group because of solution cavities and fractures, and intergranular in the Jordan Sandstone. Water in the aquifer is confined except in the eastern part. Water generally flows to the north and east into the Minnesota and Mississippi Rivers. A ground-water divide separates part of the flow southward into Iowa. This aquifer supplies more water than any other bedrock one in the State.
Calcium magnesium bicarbonate type water is most common in the aquifer. Calcium and sulfate and, to a lesser degree sodium and magnesium, increase in concentration toward the southwestern part of the study area. Bicarbonate concentration, on the other hand, decreases toward the southwestern corner of the study area. Leakage from overlying Cretaceous deposits is the source of much of the sulfate and other minerals in the southwest.
This report is one of a series on the hydrogeology and water quality of the 14 principal aquifers in Minnesota prepared by the U. S. Geological Survey. The U. S. Environmental Protection Agency requested these studies because of the need for information to develop its Underground Injection Control Program.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri834045","collaboration":"Prepared in cooperation with the U.S. Environmental Protection Agency","usgsCitation":"Ruhl, J.F., Wolf, R.J., and Adolphson, D.G., 1983, Hydrogeologic and water-quality characteristics of the Prairie du Chien-Jordan aquifer, Southeast Minnesota: U.S. Geological Survey Water-Resources Investigations Report 83-4045, 2 Plates: 39.28 x 33.33 inches and 39.08 x 33.41 inches, https://doi.org/10.3133/wri834045.","productDescription":"2 Plates: 39.28 x 33.33 inches and 39.08 x 33.41 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":170272,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":414057,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_35685.htm","linkFileType":{"id":5,"text":"html"}},{"id":81880,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1983/4045/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":81879,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1983/4045/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Minnesota","otherGeospatial":"Prairie du Chien-Jordan aquifer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -92.8619384765625,\n 45.71385093029221\n ],\n [\n -93.3837890625,\n 45.706179285330855\n ],\n [\n -93.8507080078125,\n 45.65628792636447\n ],\n [\n -94.207763671875,\n 45.583289756006316\n ],\n [\n -94.3011474609375,\n 45.46783598133375\n ],\n [\n -94.39453125,\n 45.232349197513116\n ],\n [\n -94.537353515625,\n 45.058001435398296\n ],\n [\n -94.7186279296875,\n 44.85197466334987\n ],\n [\n -94.89990234375,\n 44.629573191951046\n ],\n [\n -94.976806640625,\n 44.53959000445632\n ],\n [\n -95.3118896484375,\n 44.465151013519616\n ],\n [\n -95.4052734375,\n 44.296332880058706\n ],\n [\n -95.3118896484375,\n 44.12702800650004\n ],\n [\n -94.97131347656249,\n 43.91768033000405\n ],\n [\n -94.8944091796875,\n 43.504736854976954\n ],\n [\n -91.23046875,\n 43.504736854976954\n ],\n [\n -91.219482421875,\n 43.57243174740972\n ],\n [\n -91.2799072265625,\n 43.628123412124616\n ],\n [\n -91.241455078125,\n 43.75522505306928\n ],\n [\n -91.263427734375,\n 43.83452678223684\n ],\n [\n -91.3897705078125,\n 43.96909818325174\n ],\n [\n -91.461181640625,\n 44.008620115415354\n ],\n [\n -91.5655517578125,\n 44.03232064275084\n ],\n [\n -91.636962890625,\n 44.06390660801779\n ],\n [\n -91.73583984374999,\n 44.11125397357153\n ],\n [\n -91.8402099609375,\n 44.18614312298759\n ],\n [\n -91.8896484375,\n 44.24913396886894\n ],\n [\n -91.9500732421875,\n 44.32384807250689\n ],\n [\n -91.9720458984375,\n 44.35527821160296\n ],\n [\n -92.1148681640625,\n 44.41416430998939\n ],\n [\n -92.21923828124999,\n 44.44554600843547\n ],\n [\n -92.31262207031249,\n 44.49650533109348\n ],\n [\n -92.31262207031249,\n 44.53959000445632\n ],\n [\n -92.5048828125,\n 44.574817404670306\n ],\n [\n -92.57080078125,\n 44.59829048984011\n ],\n [\n -92.6641845703125,\n 44.65693173288727\n ],\n [\n -92.8070068359375,\n 44.750634493861064\n ],\n [\n -92.74658203125,\n 44.85586880735725\n ],\n [\n -92.7630615234375,\n 44.90646871709883\n ],\n [\n -92.74658203125,\n 44.94536144236941\n ],\n [\n -92.7850341796875,\n 45.03859654645257\n ],\n [\n -92.79602050781249,\n 45.06964120886863\n ],\n [\n -92.74108886718749,\n 45.11230010229608\n ],\n [\n -92.7630615234375,\n 45.178164812206376\n ],\n [\n -92.757568359375,\n 45.27488643704894\n ],\n [\n -92.691650390625,\n 45.36372498305678\n ],\n [\n -92.6641845703125,\n 45.398449976304086\n ],\n [\n -92.6531982421875,\n 45.463983441272745\n ],\n [\n -92.6751708984375,\n 45.48324350868221\n ],\n [\n -92.7191162109375,\n 45.533288879467456\n ],\n [\n -92.7630615234375,\n 45.56021795715051\n ],\n [\n -92.8179931640625,\n 45.56021795715051\n ],\n [\n -92.88940429687499,\n 45.57175504130605\n ],\n [\n -92.8729248046875,\n 45.6178796835697\n ],\n [\n -92.8619384765625,\n 45.71385093029221\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a50e4b07f02db628d15","contributors":{"authors":[{"text":"Ruhl, J. F.","contributorId":81866,"corporation":false,"usgs":true,"family":"Ruhl","given":"J.","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":229896,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wolf, R. J.","contributorId":21518,"corporation":false,"usgs":true,"family":"Wolf","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":229895,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Adolphson, D. G.","contributorId":106081,"corporation":false,"usgs":true,"family":"Adolphson","given":"D.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":229897,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70180857,"text":"70180857 - 1983 - Use of nearshore and estuarine areas by gray whales (Eschrichtius robustus) in the eastern Bering Sea","interactions":[],"lastModifiedDate":"2018-05-20T11:33:37","indexId":"70180857","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":894,"text":"Arctic","active":true,"publicationSubtype":{"id":10}},"title":"Use of nearshore and estuarine areas by gray whales (Eschrichtius robustus) in the eastern Bering Sea","docAbstract":"During spring aerial surveys of the coast of the southeastern Bering Sea significant numbers of gray whales were seen in nearshore waters along the north side of the Alaska Peninsula. Many (50-80%) of these animals were observed surfacing with mud trails or lying on their sides, characteristics both associated with feeding. A migration route close to shore (within 1-2 km) was used until whales neared Egegik Bay, where they began to head west 5-8 km offshore, across northern Bristol Bay. Smaller numbers of gray whales were present throughout summer in nearshore waters and estuaries along the north side of the Alaska Peninsula. At Nelson Lagoon gray whales normally used the lagoon in spring, were absent during early summer, returned in mid-summer, and then were present until late November when they departed for the wintering grounds. Gray whales were present in the lagoon most often during periods of peak tidal flow; those that appeared to be feeding were oriented into the current. Three behaviors that appeared to be associated with feeding were observed: side-feeding from a stationary position within shallow waters of lagoon channels, diving within the lagoon and in nearshore waters, and elliptical side-feeding in the surf zone along the outer coast. Large crustaceans of the genus Crangon were available to and probably eaten by gray whales at Nelson Lagoon.
","language":"English","publisher":"Arctic Institute of North America","publisherLocation":"Calgary, AB","doi":"10.14430/arctic2276","usgsCitation":"Gill, R., and Hall, J.D., 1983, Use of nearshore and estuarine areas by gray whales (Eschrichtius robustus) in the eastern Bering Sea: Arctic, v. 36, no. 3, p. 275-281, https://doi.org/10.14430/arctic2276.","productDescription":"7 p.","startPage":"275","endPage":"281","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true},{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"links":[{"id":480225,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.14430/arctic2276","text":"Publisher Index Page"},{"id":334784,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Bering Sea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -167.03613281249997,\n 54.08517342088679\n ],\n [\n -167.03613281249997,\n 59.80063426102869\n ],\n [\n -154.3359375,\n 59.80063426102869\n ],\n [\n -154.3359375,\n 54.08517342088679\n ],\n [\n -167.03613281249997,\n 54.08517342088679\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"36","issue":"3","noUsgsAuthors":false,"publicationDate":"1983-01-01","publicationStatus":"PW","scienceBaseUri":"589847abe4b0efcedb7072e5","contributors":{"authors":[{"text":"Gill, Robert E. Jr. 0000-0002-6385-4500 rgill@usgs.gov","orcid":"https://orcid.org/0000-0002-6385-4500","contributorId":171747,"corporation":false,"usgs":true,"family":"Gill","given":"Robert E.","suffix":"Jr.","email":"rgill@usgs.gov","affiliations":[{"id":117,"text":"Alaska Science Center Biology WTEB","active":true,"usgs":true}],"preferred":true,"id":662612,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hall, John D. 0000-0002-7670-5459","orcid":"https://orcid.org/0000-0002-7670-5459","contributorId":179094,"corporation":false,"usgs":false,"family":"Hall","given":"John","email":"","middleInitial":"D.","affiliations":[{"id":28155,"text":"Century Engineering, Anchorage, AK","active":true,"usgs":false}],"preferred":false,"id":662613,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70185414,"text":"70185414 - 1983 - Nestling growth relationships of brown-headed cowbirds and dickcissels ","interactions":[],"lastModifiedDate":"2017-03-23T11:24:00","indexId":"70185414","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"Nestling growth relationships of brown-headed cowbirds and dickcissels ","docAbstract":"Data on nestling growth of brood parasites and their hosts are surprisingly few in the literature, Even the Brown-headed Cowbird (Molothrus ater), whose host relations have been studied in some other respects, has not been studied in any detail from this standpoint. This is particularly regrettable because the lack of host specialization and high incidence of multiple parasitism in this species recommend it for intensive studies of parasite-host growth relationships. Isolated or fragmentary records of growth in cowbirds are available in Friedman (The Cowbirds, C. C. Thomas, Springfield, Illinois, 1929), Pickwell (Trans, Acad. Sci. St. Louis 27:1-160, 1931), Herrick Wild Birds at Home, Appleton-Century, New York, New York, 1935), Nice (Trans. Linn. Soc. N.Y. 4, 1937; Wilson Bull. 51:233-239, 1939), Mayfield (The Kirtland's Warbler, Cranbrook Inst, Sci., Illinois, 1960), and Nolan (Ornithol, Monor, No. 26. 1978). Hann (Wilson Bull. 49:145-237. 1937) illustrated the growth of five cowbirds raised in three nests of the Ovenbird (Seiurus aurocapillus), Norris Wilson Bull, 59-83-103, 1947) provided data for five individuals raised by different host species, and Scott (Wilson Bull, 91:464-466, 1979) presented pooled growth data for nine individuals raised by three different host species. King (Auk 90:19-34, 1973) measured the growth of Shiny Cowbirds (Molothrus bonariensis) in nests of Rufous-collared Sparrows (Zonotrichia capensis) and found that broods of two cowbirds grew at a substantially slower rate than broods of one, He suggested that Z. capensis could rear a maximum of two cowbirds or four sparrows, or an equivalent combination.
In 1974 collected data on the growth relationships of Brown-headed Cowbirds and Dickcissels (Spiza americana) in prairie habitat in eastern Kansas (Konza Prairie Research Natural Area). The intensity of cowbird parasitism in this study was extremely high - I found nests containing as many as nine cowbird eggs and three host eggs, More than one cowbird was evidently laying in many of the nests, behavior that may present some intricate evolutionary problems with respect to clutch-size manipulation by cowbirds. Fifty-nine of 65 nests were parasitized 91%, and the mean number of cowbird eggs per parasitized nest was 3.1 (SD 1.74). Dickcissels raised up to five young in mixed broods of various composition. Brood composition at fledging in 27 successful nests (42% of the total) averaged 1.6 Dickcissels and 1.3 cowbirds.
Active thermal areas are concentrated in three areas on Mauna Loa and three areas on Kilauea. High-temperature fumaroles (115-362°C) on Mauna Loa are restricted to the summit caldera, whereas high-temperature fumaroles on Kilauea are found in the upper East Rift Zone (Mauna Ulu summit fumaroles, 562°C), middle East Rift Zone (1977 eruptive fissure fumaroles), and in the summit caldera. Solfataric activity that has continued for several decades occurs along border faults of Kilauea caldera and at Sulphur Cone on the southwest rift zone of Mauna Loa. Solfataras that are only a few years old occur along recently active eruptive fissures in the summit caldera and along the rift zones of Kilauea. Steam vents and hot-air cracks also occur at the edges of cooling lava ponds, on the summits of lava shields, along faults and graben fractures, and in diffuse patches that may reflect shallow magmatic intrusions.
","language":"English","publisher":"Elsevier Science","doi":"10.1016/0377-0273(83)90028-8","issn":"03770273","usgsCitation":"Casadevall, T.J., and Hazlett, R.W., 1983, Thermal areas on Kilauea and Mauna Loa Volcanoes, Hawaii: Journal of Volcanology and Geothermal Research, v. 16, no. 3-4, p. 173-188, https://doi.org/10.1016/0377-0273(83)90028-8.","productDescription":"16 p.","startPage":"173","endPage":"188","costCenters":[],"links":[{"id":221361,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.5,\n 19.25\n ],\n [\n -155,\n 19.25\n ],\n [\n -155,\n 19.5\n ],\n [\n -155.5,\n 19.5\n ],\n [\n -155.5,\n 19.25\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"16","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb211e4b08c986b32559a","contributors":{"authors":[{"text":"Casadevall, Thomas J. 0000-0002-9447-6864 tcasadevall@usgs.gov","orcid":"https://orcid.org/0000-0002-9447-6864","contributorId":2734,"corporation":false,"usgs":true,"family":"Casadevall","given":"Thomas","email":"tcasadevall@usgs.gov","middleInitial":"J.","affiliations":[{"id":35995,"text":"Geology, Geophysics, and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":360953,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hazlett, Richard W.","contributorId":89201,"corporation":false,"usgs":true,"family":"Hazlett","given":"Richard","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":360952,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":46989,"text":"ofr821030 - 1983 - Geologic map of the Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Range quadrangles, Pondera and Glacier Counties, Montana","interactions":[],"lastModifiedDate":"2023-08-25T18:26:40.347672","indexId":"ofr821030","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"82-1030","title":"Geologic map of the Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Range quadrangles, Pondera and Glacier Counties, Montana","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr821030","usgsCitation":"Mudge, M.R., Earhart, R., Perry, W.J., and Bohannon, R.G., 1983, Geologic map of the Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Range quadrangles, Pondera and Glacier Counties, Montana: U.S. Geological Survey Open-File Report 82-1030, 1 Plate: 34.92 x 32.46 inches, https://doi.org/10.3133/ofr821030.","productDescription":"1 Plate: 34.92 x 32.46 inches","costCenters":[],"links":[{"id":108422,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13625.htm","linkFileType":{"id":5,"text":"html"},"description":"13625"},{"id":83892,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1982/1030/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":172698,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Montana","county":"Glacier County, Pondera County","otherGeospatial":"Mitten Lake, Half Dome Crag, Hyde Creek, East Glacier Park, Big Rock, and Magee Ranch quadrangles","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -113.25,\n 48.5\n ],\n [\n -113.25,\n 48.25\n ],\n [\n -112.875,\n 48.25\n ],\n [\n -112.875,\n 48.5\n ],\n [\n -113.25,\n 48.5\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696904","contributors":{"authors":[{"text":"Mudge, Melville Rhodes","contributorId":77119,"corporation":false,"usgs":true,"family":"Mudge","given":"Melville","email":"","middleInitial":"Rhodes","affiliations":[],"preferred":false,"id":234447,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Earhart, R.L.","contributorId":73175,"corporation":false,"usgs":true,"family":"Earhart","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":234446,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Perry, W. J. Jr.","contributorId":64266,"corporation":false,"usgs":true,"family":"Perry","given":"W.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":234445,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bohannon, R. G.","contributorId":61808,"corporation":false,"usgs":true,"family":"Bohannon","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":234444,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":21016,"text":"ofr8333 - 1983 - Hydrology of area 6, Eastern Coal Province, Maryland, West Virginia and Pennsylvania","interactions":[],"lastModifiedDate":"2023-03-29T19:53:53.242091","indexId":"ofr8333","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"83-33","title":"Hydrology of area 6, Eastern Coal Province, Maryland, West Virginia and Pennsylvania","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr8333","usgsCitation":"Staubitz, W., and Sobashinski, J.R., 1983, Hydrology of area 6, Eastern Coal Province, Maryland, West Virginia and Pennsylvania: U.S. Geological Survey Open-File Report 83-33, 131 p., https://doi.org/10.3133/ofr8333.","productDescription":"131 p.","costCenters":[],"links":[{"id":414908,"rank":3,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_13985.htm","linkFileType":{"id":5,"text":"html"}},{"id":153732,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0033/report-thumb.jpg"},{"id":95445,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0033/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Maryland, Pennsylvania, West Virginia","otherGeospatial":"Eastern Coal Province","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -79.488,\n 39.958\n ],\n [\n -79.488,\n 39.071\n ],\n [\n -78.558,\n 39.071\n ],\n [\n -78.558,\n 39.958\n ],\n [\n -79.488,\n 39.958\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a13e4b07f02db601f58","contributors":{"authors":[{"text":"Staubitz, W. W.","contributorId":73209,"corporation":false,"usgs":true,"family":"Staubitz","given":"W. W.","affiliations":[],"preferred":false,"id":183688,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sobashinski, John R.","contributorId":16856,"corporation":false,"usgs":true,"family":"Sobashinski","given":"John","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":183687,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70184434,"text":"70184434 - 1983 - Populations and habitat use of marine birds in the Semidi Islands, Alaska","interactions":[],"lastModifiedDate":"2017-03-08T15:27:08","indexId":"70184434","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2793,"text":"Murrelet","active":true,"publicationSubtype":{"id":10}},"title":"Populations and habitat use of marine birds in the Semidi Islands, Alaska","docAbstract":"About one-quarter of the resident seabirds in the Gulf of Alaska breed on the Semidi Islands. In terms of biomass, the proportion is closer to one-third. The most abundant birds are Common and Thick-billed Murres, with a combined population exceeding 1 million birds. Hundreds of thousands of Horned Puffins breed in burrows on two islands. Other species numbering more than 100,000 individuals include the Northern Fulmar, Fork-tailed and Leach's Storm-Petrels, and possibly also the Black-legged Kittiwake and Tufted Puffin. Both species of storm-petrels commonly nest in side chambers of puffin burrows. Parasitic Jaegers nest in a loose colony on Chowiet Island. This behavior has not been reported elsewhere in the Gulf of Alaska. Red-faced and Pelagic Cormorants commonly change breeding colony location from year to year. The Semidi Islands are the easternmost breeding site for Least Auklets.
","language":"English","publisher":"Society for Northwestern Vertebrate Biology","doi":"10.2307/3534688","usgsCitation":"Hatch, S.A., and Hatch, M.A., 1983, Populations and habitat use of marine birds in the Semidi Islands, Alaska: Murrelet, v. 64, no. 2, p. 39-46, https://doi.org/10.2307/3534688.","productDescription":"8 p.","startPage":"39","endPage":"46","costCenters":[{"id":114,"text":"Alaska Science Center","active":true,"usgs":true}],"links":[{"id":337134,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Gulf of Alaska, Semidi Islands","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -156.91978454589844,\n 55.96419132294944\n ],\n [\n -156.55792236328122,\n 55.96419132294944\n ],\n [\n -156.55792236328122,\n 56.25441316154926\n ],\n [\n -156.91978454589844,\n 56.25441316154926\n ],\n [\n -156.91978454589844,\n 55.96419132294944\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"64","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58c12664e4b014cc3a3d353d","contributors":{"authors":[{"text":"Hatch, Scott A. 0000-0002-0064-8187 shatch@usgs.gov","orcid":"https://orcid.org/0000-0002-0064-8187","contributorId":2625,"corporation":false,"usgs":true,"family":"Hatch","given":"Scott","email":"shatch@usgs.gov","middleInitial":"A.","affiliations":[{"id":116,"text":"Alaska Science Center Biology MFEB","active":true,"usgs":true}],"preferred":true,"id":681476,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hatch, Martha A.","contributorId":181576,"corporation":false,"usgs":false,"family":"Hatch","given":"Martha","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":681477,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011370,"text":"70011370 - 1983 - Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A.","interactions":[],"lastModifiedDate":"2018-10-24T16:06:30","indexId":"70011370","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2499,"text":"Journal of Volcanology and Geothermal Research","active":true,"publicationSubtype":{"id":10}},"title":"Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A.","docAbstract":"New investigations of the geology of Crater Lake National Park necessitate a reinterpretation of the eruptive history of Mount Mazama and of the formation of Crater Lake caldera. Mount Mazama consisted of a glaciated complex of overlapping shields and stratovolcanoes, each of which was probably active for a comparatively short interval. All the Mazama magmas apparently evolved within thermally and compositionally zoned crustal magma reservoirs, which reached their maximum volume and degree of differentiation in the climactic magma chamber ∼ 7000 yr B.P.
The history displayed in the caldera walls begins with construction of the andesitic Phantom Cone ∼ 400,000 yr B.P. Subsequently, at least 6 major centers erupted combinations of mafic andesite, andesite, or dacite before initiation of the Wisconsin Glaciation ∼ 75,000 yr B.P. Eruption of andesitic and dacitic lavas from 5 or more discrete centers, as well as an episode of dacitic pyroclastic activity, occurred until ∼ 50,000 yr B.P.; by that time, intermediate lava had been erupted at several short-lived vents. Concurrently, and probably during much of the Pleistocene, basaltic to mafic andesitic monogenetic vents built cinder cones and erupted local lava flows low on the flanks of Mount Mazama. Basaltic magma from one of these vents, Forgotten Crater, intercepted the margin of the zoned intermediate to silicic magmatic system and caused eruption of commingled andesitic and dacitic lava along a radial trend sometime between ∼ 22,000 and ∼ 30,000 yr B.P. Dacitic deposits between 22,000 and 50,000 yr old appear to record emplacement of domes high on the south slope. A line of silicic domes that may be between 22,000 and 30,000 yr old, northeast of and radial to the caldera, and a single dome on the north wall were probably fed by the same developing magma chamber as the dacitic lavas of the Forgotten Crater complex. The dacitic Palisade flow on the northeast wall is ∼ 25,000 yr old. These relatively silicic lavas commonly contain traces of hornblende and record early stages in the development of the climatic magma chamber.
Some 15,000 to 40,000 yr were apparently needed for development of the climactic magma chamber, which had begun to leak rhyodacitic magma by 7015 ± 45 yr B.P. Four rhyodacitic lava flows and associated tephras were emplaced from an arcuate array of vents north of the summit of Mount Mazama, during a period of ∼ 200 yr before the climactic eruption. The climactic eruption began 6845 ± 50 yr B.P. with voluminous airfall deposition from a high column, perhaps because ejection of ∼ 4−12 km3 of magma to form the lava flows and tephras depressurized the top of the system to the point where vesiculation at depth could sustain a Plinian column. Ejecta of this phase issued from a single vent north of the main Mazama edifice but within the area in which the caldera later formed. The Wineglass Welded Tuff of Williams (1942) is the proximal featheredge of thicker ash-flow deposits downslope to the north, northeast, and east of Mount Mazama and was deposited during the single-vent phase, after collapse of the high column, by ash flows that followed topographic depressions. Approximately 30 km3 of rhyodacitic magma were expelled before collapse of the roof of the magma chamber and inception of caldera formation ended the single-vent phase. Ash flows of the ensuing ring-vent phase erupted from multiple vents as the caldera collapsed. These ash flows surmounted virtually all topographic barriers, caused significant erosion, and produced voluminous deposits zoned from rhyodacite to mafic andesite. The entire climactic eruption and caldera formation were over before the youngest rhyodacitic lava flow had cooled completely, because all the climactic deposits are cut by fumaroles that originated within the underlying lava, and part of the flow oozed down the caldera wall.
A total of ∼ 51−59 km3 of magma was ejected in the precursory and climactic eruptions, and ∼ 40−52 km3 of Mount Mazama was lost by caldera formation. The spectacular compositional zonation shown by the climactic ejecta — rhyodacite followed by subordinate andesite and mafic andesite — reflects partial emptying of a zoned system, halted when the crystal-rich magma became too viscous for explosive fragmentation. This zonation was probably brought about by convective separation of low-density, evolved magma from underlying mafic magma. Confinement of postclimactic eruptive activity to the caldera attests to continuing existence of the Mazama magmatic system.
","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Journal of Volcanology and Geothermal Research","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1016/0377-0273(83)90004-5","issn":"03770273","usgsCitation":"Bacon, C., 1983, Eruptive history of Mount Mazama and Crater Lake Caldera, Cascade Range, U.S.A.: Journal of Volcanology and Geothermal Research, v. 18, no. 1-4, p. 57-115, https://doi.org/10.1016/0377-0273(83)90004-5.","productDescription":"59 p.","startPage":"57","endPage":"115","numberOfPages":"59","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":221285,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Mount Mazama, Crater Lake, Cascade Range","volume":"18","issue":"1-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0a57e4b0c8380cd522f6","contributors":{"authors":[{"text":"Bacon, C. R. 0000-0002-2165-5618","orcid":"https://orcid.org/0000-0002-2165-5618","contributorId":21522,"corporation":false,"usgs":true,"family":"Bacon","given":"C. R.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":false,"id":360936,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011617,"text":"70011617 - 1983 - Structure, burial history, and petroleum potential of frontal thrust belt and adjacent foreland, southwest Montana","interactions":[],"lastModifiedDate":"2023-01-11T12:43:49.73678","indexId":"70011617","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Structure, burial history, and petroleum potential of frontal thrust belt and adjacent foreland, southwest Montana","docAbstract":"The frontal thrust belt in the Lima area of southwestern Montana consists of blind (nonsurfacing) thrusts of the Lima thrust system beneath the Lima anticline and the Tendoy thrust sheet to the west. The Tendoy sheet involves Mississippian through Cretaceous rocks of the southwest-plunging nose of the Mesozoic Blacktail-Snowcrest uplift that are thrust higher (northeast) onto the uplift. The front of the Tendoy sheet west of Lima locally has been warped by later compressive deformation which also involved synorogenic conglomerates of the structurally underlying Beaverhead Formation. To the north, recent extension faulting locally has dropped the front of the Tendoy sheet beneath Quaternary gravels. Rocks of the exposed Tendoy sheet have never been deeply buried, based on itrinite reflectance of <= 0.6%, conodont CAI (color alteration index) values that are uniformly 1, and on supporting organic geochemical data from Paleozoic rocks from the Tendoy thrust sheet. Directly above and west of the Tendoy sheet lie formerly more deeply buried rocks of the Medicine Lodge thrust system. Their greater burial depth is indicated by higher conodont CAI values. West-dipping post-Paleocene extension faults truncate much of the rear part of the Tendoy sheet and also separate the Medicine Lodge sheet from thrust sheets of the Beaverhead Range still farther west.
The Laramide Blacktail-Snowcrest uplift east of the frontal thrust belt is asymmetric. Its southeast, steeper limb is exposed along the Snowcrest Range. This limb extends southwestward in the complexly deformed Snowcrest structural terrane. Northwest-dipping thrusts on this limb involve basement rocks and probably merge with depth into a major sub-Snowcrest Range thrust. This major thrust borders and is chiefly responsible for the Blacktail-Snowcrest uplift and adjacent Ruby synclinorium to the southeast. Uniform conodont CAI values of 1 from both the southeast and northwest flanks of the Blacktail-Snowcrest uplift indicate that no thick cover of Upper Cretaceous or younger rocks extended over the flanks of the uplift. During Mississippian through Permian time, the area of later Laram de uplift underwent more rapid subsidence than the area of the Laramide Ruby syncline and the Centennial basin to the southeast. The inferred sub-Snowcrest Range thrust fault apparently represents a reactivated zone of basement weakness.
The intersection of thrust-belt and foreland trends, similar to the Uinta uplift area to the south, probably formed a number of structural traps for hydrocarbons which have not yet been tested. Potential petroleum source beds and reservoir rocks are both present in southwest Montana. However, remnants of Tertiary lava flows through much of the area, Tertiary to recent basin-and-range faulting, and supermaturity with respect to oil of Permian and older rocks in the western Centennial uplift area are additional factors which must be considered in any estimate of hydrocarbon potential of the Cordilleran overthrust belt and adjacent foreland in extreme southwestern Montana.
","language":"English","publisher":"American Association of Petroleum Geologists","doi":"10.1306/03B5B6A0-16D1-11D7-8645000102C1865D","usgsCitation":"Perry, W.J., Wardlaw, B.R., Bostick, N.H., and Maughan, E.K., 1983, Structure, burial history, and petroleum potential of frontal thrust belt and adjacent foreland, southwest Montana: American Association of Petroleum Geologists Bulletin, v. 67, no. 5, p. 725-743, https://doi.org/10.1306/03B5B6A0-16D1-11D7-8645000102C1865D.","productDescription":"19 p.","startPage":"725","endPage":"743","numberOfPages":"19","costCenters":[],"links":[{"id":220984,"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 \"coordinates\": [\n [\n [\n -112.5,\n 45\n ],\n [\n -112.5,\n 44.333\n ],\n [\n -112,\n 44.333\n ],\n [\n -112,\n 45\n ],\n [\n -112.5,\n 45\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"67","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b9c68e4b08c986b31d3ec","contributors":{"authors":[{"text":"Perry, W. J. Jr.","contributorId":64266,"corporation":false,"usgs":true,"family":"Perry","given":"W.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":361554,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wardlaw, B. R.","contributorId":9269,"corporation":false,"usgs":true,"family":"Wardlaw","given":"B.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":361552,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bostick, N. H.","contributorId":67099,"corporation":false,"usgs":true,"family":"Bostick","given":"N.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":361555,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Maughan, E. K.","contributorId":25568,"corporation":false,"usgs":true,"family":"Maughan","given":"E.","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":361553,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":17967,"text":"ofr83504 - 1983 - Cenozoic structural history of selected areas in the eastern Great Basin, Nevada-Utah","interactions":[],"lastModifiedDate":"2023-03-03T22:37:00.831466","indexId":"ofr83504","displayToPublicDate":"1983-01-01T00:00:00","publicationYear":"1983","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":"83-504","title":"Cenozoic structural history of selected areas in the eastern Great Basin, Nevada-Utah","docAbstract":"The Confusion Range structural trough (CRST) of west-central Utah predates the Oligocene rocks that are exposed along it. The northern part of the axial region of the CRST is complicated by structures that include reverse faults and associated folds, a large-amplitude mushroom fold, and belts of sharply flexed to overturned strata some of which are fault bounded. These structures, which also predate the Oligocene rocks, formed in a compressional regime that has been interpreted as resulting from thin-skinned gravitational gliding toward the axis of the CRST. \r\n\r\nStudy of the sparse Tertiary rocks that are scattered along the axial region of the CRST reveals abundant evidence of Oligocene and younger deformation. The chief evidence includes (1) widespread Oligocene and Miocene coarse clastic rocks, many of which are conglomerates, that attest to local and distant tectonism, (2) faults that range from high-angle structures generally with less than 100 m of normal displacement to low-angle attenuation faults some of which may have large displacements, and (3) open asymmetric folds. Together with the distribution of sheet-form bodies of ash-flow tuffs, the Oligocene stratigraphic record allows for paleogeographic reconstruction of a lacustrine basin across what is now the northern Confusion Range and one or more basins in the southern part of the CRST. The basins are inferred to have been fault controlled by reactivation of previously formed faults or steep fold flanks. They may have been localized by differential vertical movements similar to those that produced the older systems of folds and faults. Parts of early formed basins were cannibalized as local syndepositional deformation took place in the axial region of the CRST. \r\n\r\nBoth limbs of the CRST have been modified by folds that involve Oligocene rocks. Some of these folds appear to be genetically related to displacements on faults that bound them. They may record thin-skinned Neogene tectonic displacements toward the axis of the CRST. \r\n\r\nThe most intensely faulted and tilted rocks along the axis of the CRST are located in the Tunnel Spring Mountains where Miocene(?) extension on closely spaced listric faults produced as much as 70 percent extension locally. Three episodes of Oligocene-Miocene deformation, all interpreted to have formed in an extensional environment, are recognized in the Tunnel Spring Mountains. The nearby Burbank Hills area may have been involved in the same deformational episodes, though there the relationships are not as clear-cut nor does evidence occur of extreme extension. Tight asymmetric folds in the Burbank Hills are interpreted as drape structures formed over buried normal faults. Other structures along the southern CRST have fold-like forms, but they result from cross-strike alternations in fault-related tilt directions, and they formed in an extensional stress regime. Least-principal stress directions inferred from orientations of extensional structures vary from ENE-WSW in the southern Tunnel Spring Mountains to approximately E-W in the Disappointment Hills and NW-SE in selected areas east of the axis of the CRST. The size, geographic distribution, and new data on the age of areas of major extensional faulting preclude previously published interpretations that the extension is related to major east-directed overthrusting of the Sevier orogeny in areas east of the hinterland of west-central Utah.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr83504","usgsCitation":"Anderson, R.E., 1983, Cenozoic structural history of selected areas in the eastern Great Basin, Nevada-Utah: U.S. Geological Survey Open-File Report 83-504, Report: i, 47 p.; 2 Plates: 19.14 x 10.65 inches and 18.40 x 15.48 inches, https://doi.org/10.3133/ofr83504.","productDescription":"Report: i, 47 p.; 2 Plates: 19.14 x 10.65 inches and 18.40 x 15.48 inches","costCenters":[],"links":[{"id":108459,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_14070.htm","linkFileType":{"id":5,"text":"html"},"description":"14070"},{"id":47206,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1983/0504/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47205,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1983/0504/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":47204,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1983/0504/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":151228,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1983/0504/report-thumb.jpg"}],"country":"United States","state":"Nevada, Utah","otherGeospatial":"eastern Great Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -114.708,\n 39.833\n ],\n [\n -114.708,\n 38.75\n ],\n [\n -113.647,\n 38.75\n ],\n [\n -113.647,\n 39.833\n ],\n [\n -114.708,\n 39.833\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6ef3","contributors":{"authors":[{"text":"Anderson, R. Ernest","contributorId":104484,"corporation":false,"usgs":true,"family":"Anderson","given":"R.","email":"","middleInitial":"Ernest","affiliations":[],"preferred":false,"id":178298,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70135757,"text":"70135757 - 1983 - Crustal structure beneath the southern Appalachians: Nonuniqueness of gravity modeling","interactions":[],"lastModifiedDate":"2017-08-24T12:56:52","indexId":"70135757","displayToPublicDate":"1982-12-27T00:00:00","publicationYear":"1983","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1796,"text":"Geology","active":true,"publicationSubtype":{"id":10}},"title":"Crustal structure beneath the southern Appalachians: Nonuniqueness of gravity modeling","docAbstract":"Gravity models computed for a profile across the long-wavelength paired negative-positive Bouguer anomalies of the southern Appalachian Mountains show that the large negative anomaly can be explained by a crustal root zone, whereas the steep gradient and positive anomaly east of the root may be explained equally well by three different geometries: a suture zone, a mantle upwarp, or a shallow body. Seismic data support the existence of a mountain root but are inadequate to resolve differences among the three possible geometries for the positive anomaly. The presence of outcropping mafic and ultramafic rocks in the southern Appalachians and the inferred tectonic history of the Appalachian orogen are most consistent with the suture-zone model. Crust similar to continental crust probably exists beneath the Coastal Plain and inner continental shelf where the gravity anomalies return to near-zero values.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0091-7613(1983)11<611:CSBTSA>2.0.CO;2","usgsCitation":"Hutchinson, D.R., Grow, J., and Klitgord, K.D., 1983, Crustal structure beneath the southern Appalachians: Nonuniqueness of gravity modeling: Geology, v. 11, no. 10, p. 611-615, https://doi.org/10.1130/0091-7613(1983)11<611:CSBTSA>2.0.CO;2.","productDescription":"5 p.","startPage":"611","endPage":"615","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true}],"links":[{"id":296724,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Appalachian Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -69.01611328125,\n 47.502358951968596\n ],\n [\n -66.6650390625,\n 45.336701909968106\n ],\n [\n -86.484375,\n 31.82156451492074\n ],\n [\n -88.2861328125,\n 33.65120829920497\n ],\n [\n -69.01611328125,\n 47.502358951968596\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"11","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"549165bfe4b0d0759afaad80","contributors":{"authors":[{"text":"Hutchinson, Deborah R. 0000-0002-2544-5466 dhutchinson@usgs.gov","orcid":"https://orcid.org/0000-0002-2544-5466","contributorId":521,"corporation":false,"usgs":true,"family":"Hutchinson","given":"Deborah","email":"dhutchinson@usgs.gov","middleInitial":"R.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":536831,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Grow, John A.","contributorId":51739,"corporation":false,"usgs":true,"family":"Grow","given":"John A.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":536832,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Klitgord, Kim D.","contributorId":82307,"corporation":false,"usgs":true,"family":"Klitgord","given":"Kim","email":"","middleInitial":"D.","affiliations":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"preferred":false,"id":536833,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":30342,"text":"wri8159 - 1982 - Effects of land use on surface-water quality in the East Everglades, Dade County, Florida","interactions":[],"lastModifiedDate":"2021-12-13T12:29:37.561555","indexId":"wri8159","displayToPublicDate":"2021-12-12T20:45:00","publicationYear":"1982","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":"81-59","title":"Effects of land use on surface-water quality in the East Everglades, Dade County, Florida","docAbstract":"Water-quality characteristics were determined at five developed areas in the East Everglades, Dade County, Florida, during the 1978 wet season (June through October). These areas are designated as: Coopertown; Chekika Hammock State Park; residential area; rock-plowed tomato field; and Cracker Jack Slough agricultural area. Data from the developed areas were compared with data from four baseline sites in undeveloped areas to determine the effects of land use on the surface-water quality. The rock-plowed tomato field was the only area where surface-water quality was affected. Water quality at this field is affected by agricultural activities and chemical applications as indicated by increased concentrations of orthophosphate, organic nitrogen, organic carbon, copper, manganese, mercury, and potassium. The remaining four areas of land use had water-quality characteristics typical of baseline sites in nearby Northeast Shark River Slough or Taylor Slough. Chemical analyses of soil indicated chlorinated-hydrocarbon insecticide residues at Coopertown and the two agricultural areas, Cracker Jack Slough and the rock-plowed tomato field. Trace elements in concentrations greater than base level occurred at both agricultural areas (manganese), Chekika Hammock State Park (manganese), and at Coopertown (lead and zinc). (USGS)","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/wri8159","collaboration":"Prepared in cooperation with the Metropolitan Dade County Planning Department","usgsCitation":"Waller, B.G., 1982, Effects of land use on surface-water quality in the East Everglades, Dade County, Florida: U.S. Geological Survey Water-Resources Investigations Report 81-59, Report: v, 37 p.; 2 Plates: 32.88 x 30.00 inches or smaller, https://doi.org/10.3133/wri8159.","productDescription":"Report: v, 37 p.; 2 Plates: 32.88 x 30.00 inches or smaller","costCenters":[{"id":27821,"text":"Caribbean-Florida Water Science Center","active":true,"usgs":true}],"links":[{"id":159305,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wri/1981/0059/coverthb.jpg"},{"id":59135,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1981/0059/wri8159_plate1.pdf","text":"Plate 1","size":"4.17 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":59136,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wri/1981/0059/wri8159_plate2.pdf","text":"Plate 2","size":"3.94 MB","linkFileType":{"id":1,"text":"pdf"}},{"id":2480,"rank":100,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wri/1981/0059/wri8159.pdf","text":"Report","size":"1.56 MB","linkFileType":{"id":1,"text":"pdf"},"description":"WRI 81-59"}],"country":"United States","state":"Florida","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -80.66162109375,\n 25.18505888358067\n ],\n [\n -79.98046875,\n 25.18505888358067\n ],\n [\n -79.98046875,\n 25.997549919572112\n ],\n [\n -80.66162109375,\n 25.997549919572112\n ],\n [\n -80.66162109375,\n 25.18505888358067\n ]\n ]\n ]\n }\n }\n ]\n}","contact":"Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Caribbean-Florida Water Science Center
U.S. Geological Survey
3321 College Avenue
Davie, FL 33314
Precipitation averages 47 inches per year and provides an abundant supply of water. About 20 inches returns to the atmosphere as evapotranspiration, and the remainder either flows directly to streams or percolates to the water table, eventually discharging to Long Island Sound. Small quantities of water are exported from the basin by the New Haven and Meridan Water Departments, and small quantities are imported by the New Britain Water Department and Metropolitan Direct Commission. Precipitation during 1931-60 resulted in an average annual runoff of 302 billion gallons. In inflow from the Connecticut River is added to the average annual runoff, the 4,370 billion gallon s per year is potentially available for water ue.
\nThe domestic, institutional, commercial, and industrial (other than cooling water) water use for 1970 was 7 billion gallons, which is only 3 percent of the total water used, whereas 97 percent of the total is cooling water for power plants. Approximately 60 percent of the 7 billion gallons is treated before being discharged back to the streams.
\nThe total amount of fresh water used during 1970 was estimated to be 256,000 million gallons (Mgal), of which 247,000 Mgal was used for cooling water at stream electric-generating plants. The quantity for domestic, commercial, industrial, and agricultural used was 9,000 Mgal, which was approximately 120 gallons a day per person. Public water systems providing 70 percent of these requirement and all the systems supplying water met the drinking water standards of the Connecticut General Assembly (1975).
\nTill is widespread and generally provides only small amounts of water. Wells in till normally yield only a few hundred gallons of water daily and may be inadequate during dry periods. The thickness of of till ranges from 0 to 15 feet; a median thickness of 26 feet is estimated from information provided in drillers' logs of 467 wells penetrating underlying bedrock. The till is generally used only as an emergency or secondary source of water.
\nBedrock aquifers underlie the entire area and include sedimentary and crystalline (igneous and metamorphic) rock types. These aquifers supply small and usually reliable quantities of water to wells and are the chief source of water for many rural homes and farms., About 90 percent of the wells tapping bedrock yield at least 2 gal/min. The median yields from wells tapping aquifers in sedimentary, igneous, and metamorphic rocks are 11, 8, and 6.5 gal/min, respectively.
\nThe quantity of water potentially available from stratified drift was estimated on the basis of hydraulic characteristics of the aquifers, mathematical modeling of the aquifer system, and evaluation of natural and induced recharge. Long-term yields estimated or ten areas underlain by significant thickness of stratified drift range from 0.4 to 4.4 million gallons per day (Mgal/d). A change in well spacing or numbering could increase the long-term yields, but detailed modeling verification studies are needed to confirm optimal well locations.
\nThe chemical and physical (turbidity, color, taste, and sediment load) quality of water is good. The water if generally low in dissolved solids and is classified as soft to hard. Surface water is less mineralized than ground water, especially during high flow, when it is primarily derived from surface runoff rather than groundwater runoff. A median dissolved-solids concentration of 42 milligrams per liter (mg/L) and median hardness of 18 mg/L were determined from water samples collected from 26 streams during the high-flow period. During the low-flow period, median dissolved-solids concentration of 61 mg/L and median hardness of 27 mg/L were determined from sample from the same streams.
\nThe quality of water in stratified-drift and crystalline-rock aquifers is generally better than that in the sedimentary-rock aquifers. Water from 32 wells tapping stratified drift had median dissolved-solids concentrations of 116 mg/L; and 33 wells tapping stratified drift and 42 tapping crystalline rock had median hardness of 73 mg/L and 68 mg/L, respectively. Water from 32 wells tapping sedimentary rock had median dissolved concentrations of 231 and 156 mg/L, respectively. Sedimentary rock generally yields the hardest water.
\nIron and manganese occur objectionable concentrations in places, particularly in water from streams draining swamps and in water from aquifers either rich in iron and manganese-nearing minerals or where the reducing environment for solution of these minerals is favorable. Concentrations of iron in excess of 0.3 mg/L were found in 35 percent of the high streamflow samples, and in 45 percent of the ground-water samples. Most of the high iron and manganese concentration in streams and aquifers are found east of the Connecticut River.
\n