The Pasadena earthquake (ML = 4.9) occurred on 3 December 1988, at a depth of 16 km. The hypocenters of the earthquake and its aftershocks define a east-northeast striking, steeply northwest-dipping surface that projects up to the active surficial trace of the Raymond fault. One of the nodal planes of the focal mechanism of the earthquake parallels the Raymond fault with left-lateral strike-slip movement on that plane, and is consistent with geomorphic and paleoseismic evidence that the Raymond fault is dominantly a left-lateral strike-slip fault. The existence of a component of sinistral slip along the Raymond fault had been suspected prior to the earthquake, but the northward dip of the fault and the prominent scarp along the western portion of its trace had led most workers to conclude that slip along the fault was dominantly reverse.
","language":"English","publisher":"Seismological Society of America","doi":"10.1785/BSSA0800020474","usgsCitation":"Jones, L., Sieh, K., Hauksson, E., and Hutton, L., 1990, The 3 December 1988 Pasadena, California earthquake: Evidence for strike-slip motion on the Raymond Fault: Bulletin of the Seismological Society of America, v. 80, no. 2, p. 474-482, https://doi.org/10.1785/BSSA0800020474.","productDescription":"9 p.","startPage":"474","endPage":"482","numberOfPages":"9","costCenters":[],"links":[{"id":479841,"rank":2,"type":{"id":41,"text":"Open Access External Repository Page"},"url":"https://authors.library.caltech.edu/37066/","text":"External Repository"},{"id":223244,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Pasadena","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -118.23169701853942,\n 34.241484962423115\n ],\n [\n -118.23169701853942,\n 34.081260776034796\n ],\n [\n -118.02844994822699,\n 34.081260776034796\n ],\n [\n -118.02844994822699,\n 34.241484962423115\n ],\n [\n -118.23169701853942,\n 34.241484962423115\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"80","issue":"2","noUsgsAuthors":false,"publicationDate":"1990-04-01","publicationStatus":"PW","scienceBaseUri":"505ba653e4b08c986b321067","contributors":{"authors":[{"text":"Jones, L.M.","contributorId":61433,"corporation":false,"usgs":true,"family":"Jones","given":"L.M.","email":"","affiliations":[],"preferred":false,"id":372436,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sieh, K.E.","contributorId":107303,"corporation":false,"usgs":true,"family":"Sieh","given":"K.E.","affiliations":[],"preferred":false,"id":372438,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hauksson, E.","contributorId":10932,"corporation":false,"usgs":true,"family":"Hauksson","given":"E.","affiliations":[],"preferred":false,"id":372435,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Hutton, L.K.","contributorId":66266,"corporation":false,"usgs":true,"family":"Hutton","given":"L.K.","email":"","affiliations":[],"preferred":false,"id":372437,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70016040,"text":"70016040 - 1990 - Climate factor for small-basin flood frequency","interactions":[],"lastModifiedDate":"2013-02-19T14:18:18","indexId":"70016040","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3718,"text":"Water Resources Bulletin","printIssn":"0043-1370","active":true,"publicationSubtype":{"id":10}},"title":"Climate factor for small-basin flood frequency","docAbstract":"A climate factor, CT, (T = 2-, 25-, and 100-year recurrence intervals) that delineates regional trends in small-basin flood frequency was derived using data from 71 long-term rainfall record sites. Values of CT at these sites were developed by a regression analysis that related rainfall-runoff model estimates of T-year floods to a sample set of 50 model calibrations. CT was regionalized via kriging to develop maps depicting its geographic variation for a large part of the United States east of the 105th meridian. Kriged estimates of CT and basin-runoff characteristics were used to compute regionalized T-year floods for 200 small drainage basins. Observed T-year flood estimates also were developed for these sites. Regionalized floods are shown to account for a large percentage of the variability in observed flood estimates with coefficients of determination ranging from 0.89 for 2-year floods to 0.82 for 100-year floods. The relative importance of the factors comprising regionalized flood estimates is evaluated in terms of scale (size of drainage area), basin-runoff characteristics (rainfall-runoff model parameters), and climate (CT).","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Water Resources Bulletin","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"American Water Resources Association","doi":"10.1111/j.1752-1688.1990.tb01395.x","issn":"00431370","usgsCitation":"Lichty, R., and Karlinger, M., 1990, Climate factor for small-basin flood frequency: Water Resources Bulletin, v. 26, no. 4, p. 577-586, https://doi.org/10.1111/j.1752-1688.1990.tb01395.x.","startPage":"577","endPage":"586","numberOfPages":"10","costCenters":[],"links":[{"id":222988,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":267740,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1111/j.1752-1688.1990.tb01395.x"}],"volume":"26","issue":"4","noUsgsAuthors":false,"publicationDate":"2007-06-08","publicationStatus":"PW","scienceBaseUri":"5059f651e4b0c8380cd4c6b4","contributors":{"authors":[{"text":"Lichty, R.W.","contributorId":46987,"corporation":false,"usgs":true,"family":"Lichty","given":"R.W.","affiliations":[],"preferred":false,"id":372406,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Karlinger, M.R.","contributorId":95039,"corporation":false,"usgs":true,"family":"Karlinger","given":"M.R.","affiliations":[],"preferred":false,"id":372407,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70015821,"text":"70015821 - 1990 - Precambrian terrane of north-central Wisconsin: an aeromagnetic perspective","interactions":[],"lastModifiedDate":"2023-09-21T17:33:00.578995","indexId":"70015821","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1168,"text":"Canadian Journal of Earth Sciences","active":true,"publicationSubtype":{"id":10}},"title":"Precambrian terrane of north-central Wisconsin: an aeromagnetic perspective","docAbstract":"A shaded relief magnetic map covering most of the region of exposed Precambrian rocks of north-central Wisconsin shows the structural grain and many lithologic units with clarity and comprehensive detail. The area includes part of the volcanic sequence of the Keweenawan Supergroup south of Lake Superior, the southern margin of the Archean Superior Province, the accreted island-arc terranes of the Penokean Orogen, and the Wolf River batholith. Numerous dikes are evident in the shaded relief, some being more than 200 km in length. Many of the longer dikes are reversely magnetized Keweenawan diabase associated with early extension of the Midcontinent Rift; some apparently were intruded along preexisting faults. A northwest system of dikes and faults indicated by the shaded relief map may be related to later stages of Keweenawan rifting. The Wolf River batholith is characterized by low magnetic relief associated with the predominant granitoids but includes circular plutons of highly magnetic anorthosite and a large area of magnetic rock having a signature different from the mapped anorthosite bodies. A fault bounding the western side of the batholith is paralleled by an apparent system of faults or dikes in the older terrane to the west. The magnetic map covering the Wisconsin magmatic terranes and the Archean Superior Province margin to the north is dominated by east-northeast-trending Penokean rocks. Large units of magnetic mafic rocks and less magnetic granitoid rocks are cut by a system of well-defined northeast shear zones and a more easterly trending, possibly younger set of faults, some of which contain dikes along parts of their lengths. Although the sutures bounding the magmatic terranes generally follow the magnetic trends, they do not have distinctive magnetic signatures.
","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/e90-156","issn":"00084077","usgsCitation":"King, E.R., 1990, Precambrian terrane of north-central Wisconsin: an aeromagnetic perspective: Canadian Journal of Earth Sciences, v. 27, no. 11, p. 1472-1477, https://doi.org/10.1139/e90-156.","productDescription":"6 p.","startPage":"1472","endPage":"1477","costCenters":[],"links":[{"id":223434,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Wisconsin","otherGeospatial":"Lake Superior","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -87.66671060976584,\n 44.3610017587431\n ],\n [\n -87.66671060976584,\n 46.373762217927776\n ],\n [\n -92.90108864423792,\n 46.373762217927776\n ],\n [\n -92.90108864423792,\n 44.3610017587431\n ],\n [\n -87.66671060976584,\n 44.3610017587431\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"27","issue":"11","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a8107e4b0c8380cd7b321","contributors":{"authors":[{"text":"King, E. R.","contributorId":93482,"corporation":false,"usgs":true,"family":"King","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":371848,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70016431,"text":"70016431 - 1990 - Geophysical constraints on Washington convergent margin structure","interactions":[],"lastModifiedDate":"2024-05-24T15:28:32.02146","indexId":"70016431","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":6453,"text":"Journal of Geophysical Research Solid Earth","active":true,"publicationSubtype":{"id":10}},"title":"Geophysical constraints on Washington convergent margin structure","docAbstract":"Gravity and magnetic maps of western Washington reveal the lateral structure and fabric of the Washington Coast Range, Puget Basin, and southern Washington Cascade Range. The magnetic and gravity maps show large amplitude positive anomalies associated with the shallow but largely buried section of Washington Coast Range mafic rocks which are separated by negative anomalies over deep sedimentary basins. The positive anomalies indicate that the Coast Range mafic basement extends farther east than previously thought, at least as far east as the longitude of Seattle. Linear and steep gravity and magnetic gradients indicate many unmapped, often buried faults in the Washington Coast Range Province. Magnetic highs are also associated with mapped batholiths in the Cascade arc. Several magnetic highs observed east of the Coast Range rocks and west of these batholiths may be associated with buried Tertiary plutons or ophiolites. Two-dimensional gravity and magnetic modeling constrained with geological and other geophysical data indicate that the Coast Range Province rocks are about 1 km thick at the coast, thickening to as much as 30 km near their postulated eastern edge. A maximum boundary on the average density of the upper 15–20 km of the rocks that compose the Coast Range Province of 2920 kg/m3 was established by the modeling, suggesting a composition largely of basalt and gabbro with little interbedded sediments. Under these rocks may be mantle or a subduction complex composed of dense mafic, ultramafic, and sedimentary rocks like that proposed to underlie Vancouver Island. Previous gravity models of the Washington margin include lower densities for the proposed subduction complex than for Vancouver Island, suggesting a lower component of mafic and ultramafic rocks than the rocks underlying Vancouver Island. However, my Washington model requires that the proposed subduction complex be more dense than the trench sediments and, therefore, that material denser than sediments be incorporated within it. The absence of continental mantle and the modeled wedge shape of the Coast Range Province upper crust suggest that erosion of the bottom of the overriding plate by subduction processes may have occurred.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB095iB12p19533","issn":"01480227","usgsCitation":"Finn, C.A., 1990, Geophysical constraints on Washington convergent margin structure: Journal of Geophysical Research Solid Earth, v. 95, no. B12, p. 19533-19546, https://doi.org/10.1029/JB095iB12p19533.","productDescription":"14 p.","startPage":"19533","endPage":"19546","costCenters":[],"links":[{"id":222972,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Washington","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -120.99289441326454,\n 48.94625600979734\n ],\n [\n -129.5979382121656,\n 48.94625600979734\n ],\n [\n -129.5979382121656,\n 45.56775656606118\n ],\n [\n -120.99289441326454,\n 45.56775656606118\n ],\n [\n -120.99289441326454,\n 48.94625600979734\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"95","issue":"B12","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"505a2814e4b0c8380cd59deb","contributors":{"authors":[{"text":"Finn, Carol A. 0000-0002-6178-0405 cfinn@usgs.gov","orcid":"https://orcid.org/0000-0002-6178-0405","contributorId":1326,"corporation":false,"usgs":true,"family":"Finn","given":"Carol","email":"cfinn@usgs.gov","middleInitial":"A.","affiliations":[{"id":211,"text":"Crustal Geophysics and Geochemistry Science Center","active":true,"usgs":true}],"preferred":true,"id":373492,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70137865,"text":"70137865 - 1990 - Major off-axis hydrothermal activity on the northern Gorda Ridge","interactions":[],"lastModifiedDate":"2019-12-10T13:39:05","indexId":"70137865","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1796,"text":"Geology","active":true,"publicationSubtype":{"id":10}},"title":"Major off-axis hydrothermal activity on the northern Gorda Ridge","docAbstract":"The first hydrothermal field on the northern Gorda Ridge, the Sea Cliff hydrothermal field, was discovered and geologic controls of hydrothermal activity in the rift valley were investigated on a dive series using the DSV Sea Cliff. The Sea Cliff hydrothermal field was discovered where predicted at the intersection of axis-oblique and axis-parallel faults at the south end of a linear ridge at mid-depth (2700 m) on the east wall. Preliminary mapping and sampling of the field reveal: a setting nested on nearly sediment-free fault blocks 300 m above the rift valley floor 2.6 km from the axis; a spectrum of venting types from seeps to black smokers; high conductive heat flow estimated to be equivalent to the convective flux of multiple black smokers through areas of the sea floor sealed by a caprock of elastic breccia primarily derived from basalt with siliceous cement and barite pore fillings; and a vent biota with Juan de Fuca Ridge affinites. These findings demonstrate the importance of off-axis hydrothermal activity and the role of the intersection of tectonic lineations in controlling hydrothermal sites at sea-floor spreading centers.
High-resolution seismic-reflection profiles of the Quicksands, located along a broad ridge on the platform shelf west of Key West, Florida, indicate a significant deposit of non-oolitic carbonate sand occurs in a belt 47 km long by 28 km wide. The surface of the belt is ornamented by large (5 m), migrating tidal bars, oriented in a north-south direction, on which sand waves, oriented in an east-west direction, are superimposed. Some of the sand waves are awash at low tide. The sand waves are formed by strong reversing tidal currents flowing between the Gulf of Mexico and the Straits of Florida. The waves migrate directly over Pleistocene bedrock to the east, but the deposit thickens to the west and sand waves there overlie non-oolitic Holocene accumulations as thick as 12 m. Westward-dipping accretionary bedding indicates that net migration of the sands is to the west, despite north-south movement of tidal currents. The westward edge of the accumulation has accreted over deeper, muddier deposits. Although tidal currents and resultant bedforms appear identical to those of active ooid deposits in the Bahamas and elsewhere, no oolitically coated grains were found in this study. Thin-section analyses show the principal component (average 48%) of the sands is fragmented plates of species of the green alga Halimeda , followed by particulate coral (average 17%), which increases off the flanks of the main sand body. Short vibracores confirm the presence of cross-bedding.
","language":"English","publisher":"American Geological Institute","doi":"10.1306/D4267654-2B26-11D7-8648000102C1865D","usgsCitation":"Shinn, E., Lidz, B.H., and Holmes, C.W., 1990, High-energy carbonate-sand accumulation, the Quicksands, southwest Florida Keys: Journal of Sedimentary Research, v. 60, no. 6, p. 952-967, https://doi.org/10.1306/D4267654-2B26-11D7-8648000102C1865D.","productDescription":"16 p.","startPage":"952","endPage":"967","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":186,"text":"Coastal and Marine Geology Program","active":true,"usgs":true}],"links":[{"id":297189,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida","otherGeospatial":"Florida Keys","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -83.375244140625,\n 25.334096684794456\n ],\n [\n -79.969482421875,\n 25.334096684794456\n ],\n [\n -80.04638671875,\n 24.427145340082046\n ],\n [\n -83.21044921875,\n 24.387127324604496\n ],\n [\n -83.375244140625,\n 25.334096684794456\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"60","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"54dd2bc1e4b08de9379b34ae","contributors":{"authors":[{"text":"Shinn, Eugene A.","contributorId":86708,"corporation":false,"usgs":true,"family":"Shinn","given":"Eugene A.","affiliations":[],"preferred":false,"id":538194,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lidz, Barbara H. blidz@usgs.gov","contributorId":2475,"corporation":false,"usgs":true,"family":"Lidz","given":"Barbara","email":"blidz@usgs.gov","middleInitial":"H.","affiliations":[],"preferred":true,"id":538195,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Holmes, Charles W.","contributorId":31071,"corporation":false,"usgs":true,"family":"Holmes","given":"Charles","email":"","middleInitial":"W.","affiliations":[{"id":218,"text":"Denver Federal Center","active":false,"usgs":true}],"preferred":false,"id":538196,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70015852,"text":"70015852 - 1990 - Faults of the central part of the Lewis and Clark line and fragmentation of the Late Cretaceous foreland basin in west-central Montana","interactions":[],"lastModifiedDate":"2023-12-27T12:25:44.628815","indexId":"70015852","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Faults of the central part of the Lewis and Clark line and fragmentation of the Late Cretaceous foreland basin in west-central Montana","docAbstract":"The Lewis and Clark line is a prominent zone of strike-slip, dip-slip, and oblique-slip faults that extends from near Wallace, Idaho, to east of Helena, Montana. Faults of this zone have been intermittently active from Middle Proterozoic to Holocene time, and because of numerous tectonic overprints, controversy continues about displacement directions and times of displacement along specific faults. Geologic mapping shows evidence that many principal faults of the Lewis and Clark line, such as the St. Marys-Helena Valley, Bald Butte, Ninemile, and Osburn faults, had right separation or slip that ranged between 28 and 11 km, and this displacement probably occurred during Late Cretaceous time. Other faults, such as the Elevation Mountain, Placer Creek, and Ranch Creek faults, have Late Cretaceous right separations that range between 8 and 3.2 km, and the Mount Sentinel fault zone has between 6.5 and 3 km of right separation of probable Late Cretaceous age.
Subsidiary structures of the Lewis and Clark line postdate Paleozoic and Lower Cretaceous rocks and predate Late Cretaceous stocks at some places; subsidiary faults and folds that have age constraints have slip directions compatible with right slip along adjacent, principal faults.
Sedimentation patterns of Lower and Upper Cretaceous rocks indicate that faults of the Lewis and Clark line fragmented the foredeep region of the foreland basin into separate northern and southern basins in Late Cretaceous time. The Lower and Upper Cretaceous Blackleaf Formation (Albian and lower Cenomanian) was deposited in a continuous foredeep basin that extended across the Lewis and Clark line from north of the Canadian border to southwestern Montana, a distance of about 450 km. North of the Lewis and Clark line, middle and upper Cenomanian rocks are absent, and a thin sequence of uppermost Cenomanian to Campanian rocks was deposited in a marine environment that changed to a strand-line and continental environment in early Campanian time. South of the Lewis and Clark line, middle and upper Cenomanian deposits are also absent, but a thick sequence of Turonian-to-Campanian rocks was deposited in brackish water and strand-line environments, and during later Campanian time, in a continental environment. In the region between the St. Marys-Helena Valley and Bald Butte faults, a barrier may have formed that served as a local sediment source between foredeep regions in the northern and southern foreland basin during the period 91 to 75 Ma. South of the Bald Butte fault, an extensional tectonic regime contributed to a higher sediment-accumulation rate in the foredeep region along the north border of the southern basin (30 cm/1,000 yr), as compared to lower sediment-accumulation rates (6.9 and 7.8 cm/ 1,000 yr) in the foredeep region of the south part of the northern basin.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1990)102<1021:FOTCPO>2.3.CO;2","usgsCitation":"Wallace, C.A., Lidke, D., and Schmidt, R.G., 1990, Faults of the central part of the Lewis and Clark line and fragmentation of the Late Cretaceous foreland basin in west-central Montana: Geological Society of America Bulletin, v. 102, no. 8, p. 1021-1037, https://doi.org/10.1130/0016-7606(1990)102<1021:FOTCPO>2.3.CO;2.","productDescription":"17 p.","startPage":"1021","endPage":"1037","numberOfPages":"17","costCenters":[],"links":[{"id":223131,"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 -113.93105489049955,\n 47.74152319336437\n ],\n [\n -113.93105489049955,\n 45.78512955401325\n ],\n [\n -109.9320314529997,\n 45.78512955401325\n ],\n [\n -109.9320314529997,\n 47.74152319336437\n ],\n [\n -113.93105489049955,\n 47.74152319336437\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"102","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0f27e4b0c8380cd537d2","contributors":{"authors":[{"text":"Wallace, C. A.","contributorId":15596,"corporation":false,"usgs":true,"family":"Wallace","given":"C.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":371923,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lidke, D. J.","contributorId":10857,"corporation":false,"usgs":true,"family":"Lidke","given":"D. J.","affiliations":[],"preferred":false,"id":371922,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Schmidt, R. G.","contributorId":107690,"corporation":false,"usgs":true,"family":"Schmidt","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":371924,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70016188,"text":"70016188 - 1990 - Sediment movement along the U.S. east coast continental shelf-II. Modelling suspended sediment concentration and transport rate during storms","interactions":[],"lastModifiedDate":"2018-04-09T13:20:27","indexId":"70016188","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1333,"text":"Continental Shelf Research","active":true,"publicationSubtype":{"id":10}},"title":"Sediment movement along the U.S. east coast continental shelf-II. Modelling suspended sediment concentration and transport rate during storms","docAbstract":"Long-term near-bottom wave and current observations and a one-dimensional sediment transport model are used to calculate the concentration and transport of sediment during winter storms at 60-80 m water depth along the southern flank of Georges Bank and in the Mid-Atlantic Bight. Calculations are presented for five stations, separated by more than 600 km alongshelf, that have different bottom sediment texture, bedforms and current conditions. A modified version of the sediment transport model presented by Grant and Glenn (1983, Technical Report to the American Gas Association), Glenn (1983, D.Sc. Thesis, M.I.T.), and Glenn and Grant (1987, Journal of Geophysical Research, 92, 8244-8264) is used to examine the influence of wave-current interaction, sediment stratification, and limitations on the erodibility of the bottom sediments on the concentration of sediment in the water column and on transport. Predicted suspended sediment concentrations are higher than observed, based on beam transmissometer measurements, unless an erosion limit of order a few millimeters for sediments finer than 94 ??m is imposed. The agreement between predicted and measured beam attenuation is better at stations that have significant amounts of silt plus clay in the surficial sediments than for stations with sandy sediments. Sediment concentrations during storms estimated by Moody et al. (1987, Continental Shelf Research, 7, 609-628) are within 50% of the model predictions. Sediment transport rates for sediments 94 ??m and finer are determined largely by the concentrations in the surficial sediment and the erosion depth limit. Large alongshelf transports in the direction of storm-driven currents are inferred for stations in the Mid-Atlantic Bight. During a 115-day period in winter 1979-1980, the net transport of sediment along the shelf was westward; benthic storms (defined as periods when the bottom wave stress exceeded the current stress by 2 dyn cm-2) occurred between 23 and 73% of the time, and greater than 91% of the net alongshelf transport was during storms. ?? 1990.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Continental Shelf Research","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","doi":"10.1016/0278-4343(90)90049-R","issn":"02784343","usgsCitation":"Lyne, V., Butman, B., and Grant, W., 1990, Sediment movement along the U.S. east coast continental shelf-II. Modelling suspended sediment concentration and transport rate during storms: Continental Shelf Research, v. 10, no. 5, p. 429-460, https://doi.org/10.1016/0278-4343(90)90049-R.","productDescription":"32 p.","startPage":"429","endPage":"460","costCenters":[{"id":678,"text":"Woods Hole Coastal and Marine Science Center","active":true,"usgs":true}],"links":[{"id":222838,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","otherGeospatial":"Georges Bank, Mid-Atlantic Bight","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76,\n 36\n ],\n [\n -59.58984374999999,\n 36\n ],\n [\n -59.58984374999999,\n 43\n ],\n [\n -76,\n 43\n ],\n [\n -76,\n 36\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"10","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b899ee4b08c986b316e43","contributors":{"authors":[{"text":"Lyne, V.D.","contributorId":78473,"corporation":false,"usgs":true,"family":"Lyne","given":"V.D.","email":"","affiliations":[],"preferred":false,"id":372788,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Butman, B.","contributorId":85580,"corporation":false,"usgs":true,"family":"Butman","given":"B.","email":"","affiliations":[],"preferred":false,"id":372789,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Grant, W.D.","contributorId":11764,"corporation":false,"usgs":true,"family":"Grant","given":"W.D.","email":"","affiliations":[],"preferred":false,"id":372787,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70015958,"text":"70015958 - 1990 - Contrasting soils and landscapes of the Piedmont and Coastal Plain, eastern United States","interactions":[],"lastModifiedDate":"2019-03-07T13:10:05","indexId":"70015958","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1801,"text":"Geomorphology","active":true,"publicationSubtype":{"id":10}},"title":"Contrasting soils and landscapes of the Piedmont and Coastal Plain, eastern United States","docAbstract":"The Piedmont and Coastal Plain physiographic provinces comprise 80 percent of the Atlantic Coastal states from New Jersey to Georgia. The provinces are climatically similar. The soil moisture regime is udic. The soil temperature regime is typically thermic from Virginia through Georgia, although it is mesic at altitudes above 400 m in Georgia and above 320 m in Virginia. The soil temperature regime is mesic for the Piedmont and Coastal Plain from Maryland through New Jersey. The tightly folded, structurally complex crystalline rocks of the Piedmont and the gently dipping “layer-cake” clastic sedimentary rocks and sediments of the Coastal Plain respond differently to weathering, pedogenesis, and erosion. The different responses result in two physiographically contrasting terrains; each has distinctive near-surface hydrology, regolith, drainage morphology, and morphometry.
The Piedmont is predominantly an erosional terrain. Interfluves are as narrow as 0.5 to 2 km, and are convex upward. Valleys are as narrow as 0.1 to 0.5 km and generally V-shaped in cross section. Alluvial terraces are rare and discontinuous. Soils in the Piedmont are typically less than 1 m thick, have less sand and more clay than Coastal Plain soils, and generally have not developed sandy epipedons. Infiltration rates for Piedmont soils are low at 6–15 cm/h. The soil/saprolite, soil/rock, and saprolite/rock boundaries are distinct (can be placed within 10 cm) and are characterized by ponding and/or lateral movement of water. Water movement through soil into saprolite, and from saprolite into rock, is along joints, foliation, bedding planes and faults. Soils and isotopic data indicate residence times consistent with a Pleistocene age for most Piedmont soils.
The Coastal Plain is both an erosional and a constructional terrain. Interfluves commonly are broader than 2 km and are flat. Valleys are commonly as wide as 1 km to greater than 10 km, and contain numerous alluvial and estuarine terrace sequences that can be correlated along valleys for tens of kilometers. Coastal Plain soils are typically as thick as 2 to 8 m, have high sand content throughout, and have sandy epipedons. These epipedons consist of both A and E horizons and are 1 to 4 m thick. In Coastal Plain soils, the boundaries are transitional between the solum and the underlying parent material and between weathered and unweathered parent material. Infiltration rates for Coastal Plain soils are typically higher at 13–28 cm/h, than are those for Piedmont soils. Indeed, for unconsolidated quartz sand, rates may exceed 50 cm/h. Water moves directly from the soil into the parent material through intergranularpores with only minor channelization along macropores, joints, and fractures. The comparatively high infiltration capacity results in relatively low surface runoff, and correspondingly less erosion than on the Piedmont uplands.
Due to differences in Piedmont and Coastal Plain erosion rates, topographic inversion is common along the Fall Zone; surfaces on Cenozoic sedimentary deposits of the Coastal Plain are higher than erosional surfaces on regolith weathered from late Precambrian to early Paleozoic crystalline rocks of the Piedmont. Isotopic, paleontologic, and soil data indicate that Coastal Plain surficial deposits are post-middle Miocene to Holocene in age, but most are from 5 to 2 Ma. Thus, the relatively uneroded surfaces comprise a Pliocene landscape. In the eastern third of the Coastal Plain, deposits that are less than 3.5 Ma include alluvial terraces, marine terraces and barrier/back-barrier complexes as morphostratigraphic units that cover thousands of square kilometers. Isotopic and soil data indicate that eastern Piedmont soils range from late Pliocene to Pleistocene in age, but are predominantly less than 2 Ma old. Thus, the eroded uplands of the Piedmont “peneplain” comprise a Pleistocene landscape.
","language":"English","publisher":"Elsevier","doi":"10.1016/0169-555X(90)90015-I","issn":"0169555X","usgsCitation":"Markewich, H.W., Pavich, M.J., and Buell, G.R., 1990, Contrasting soils and landscapes of the Piedmont and Coastal Plain, eastern United States: Geomorphology, v. 3, no. 3-4, p. 417-447, https://doi.org/10.1016/0169-555X(90)90015-I.","productDescription":"31 p.","startPage":"417","endPage":"447","costCenters":[],"links":[{"id":223136,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"3","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059fa7ce4b0c8380cd4db0e","contributors":{"authors":[{"text":"Markewich, Helaine W. 0000-0001-9656-3243 helainem@usgs.gov","orcid":"https://orcid.org/0000-0001-9656-3243","contributorId":2008,"corporation":false,"usgs":true,"family":"Markewich","given":"Helaine","email":"helainem@usgs.gov","middleInitial":"W.","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true}],"preferred":true,"id":372184,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Pavich, Milan J. mpavich@usgs.gov","contributorId":2348,"corporation":false,"usgs":true,"family":"Pavich","given":"Milan","email":"mpavich@usgs.gov","middleInitial":"J.","affiliations":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":372186,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Buell, Gary R. grbuell@usgs.gov","contributorId":3107,"corporation":false,"usgs":true,"family":"Buell","given":"Gary","email":"grbuell@usgs.gov","middleInitial":"R.","affiliations":[{"id":13634,"text":"South Atlantic Water Science Center","active":true,"usgs":true}],"preferred":true,"id":372185,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70016090,"text":"70016090 - 1990 - Chronologic and isotopic framework for early Proterozoic crustal evolution in the eastern Mojave Desert region, SE California","interactions":[],"lastModifiedDate":"2024-05-24T16:34:04.68862","indexId":"70016090","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2312,"text":"Journal of Geophysical Research","active":true,"publicationSubtype":{"id":10}},"title":"Chronologic and isotopic framework for early Proterozoic crustal evolution in the eastern Mojave Desert region, SE California","docAbstract":"The Early Proterozoic geologic evolution of the eastern Mojave Desert region, as defined by characteristics of its supracrustal rocks, granitoids, metamorphism, structural history, and Pb and Nd isotopic signature, contrasts sharply with other Proterozoic provinces of the southwestern United States. The oldest supracrustal rocks of the Mojave Desert region contain zircons over 2.0 Ga, corroborating Nd isotopic evidence for a much older crust here than elsewhere in the southwestern United States. Granitoids widely emplaced within these supracrustal rocks range from 1.76 to 1.64 Ga. The earlier plutons and surrounding supracrustal rocks were metamorphosed to granulite and high amphibolite facies throughout the province at about 1705 Ma in a migmatite-producing event that we term (informally) the Ivanpah orogeny. Subsequent granitoids, emplaced from 1.69 to 1.67 Ga, were voluminous along a north trending belt in the middle of the Mojave province. Younger plutons were emplaced at about 1.66 Ga in several places and at about 1.64 Ga along the extreme southern part of the province. Commonalities between the Proterozoic evolutions of the Mojave and Arizona crustal provinces do not conclusively establish the time that the provinces were juxtaposed; the data only suggest that the juxtaposition occurred between about 1.76 and 1.64 Ga.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/JB095iB12p20133","issn":"01480227","usgsCitation":"Wooden, J.L., and Miller, D., 1990, Chronologic and isotopic framework for early Proterozoic crustal evolution in the eastern Mojave Desert region, SE California: Journal of Geophysical Research, v. 95, no. B12, p. 20133-20146, https://doi.org/10.1029/JB095iB12p20133.","productDescription":"14 p.","startPage":"20133","endPage":"20146","costCenters":[],"links":[{"id":222938,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"95","issue":"B12","noUsgsAuthors":false,"publicationDate":"2012-09-20","publicationStatus":"PW","scienceBaseUri":"5059f5f2e4b0c8380cd4c4dd","contributors":{"authors":[{"text":"Wooden, J. L.","contributorId":58678,"corporation":false,"usgs":true,"family":"Wooden","given":"J.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":372516,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Miller, D. M. 0000-0003-3711-0441","orcid":"https://orcid.org/0000-0003-3711-0441","contributorId":104422,"corporation":false,"usgs":true,"family":"Miller","given":"D. M.","affiliations":[],"preferred":false,"id":372517,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70015763,"text":"70015763 - 1990 - Chemistry and origin of minor and trace elements in selected vitrinite concentrates from bituminous and anthracitic coals","interactions":[],"lastModifiedDate":"2024-02-23T00:49:29.715162","indexId":"70015763","displayToPublicDate":"1990-01-01T00:00:00","publicationYear":"1990","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2033,"text":"International Journal of Coal Geology","active":true,"publicationSubtype":{"id":10}},"title":"Chemistry and origin of minor and trace elements in selected vitrinite concentrates from bituminous and anthracitic coals","docAbstract":"Organic and inorganic affinities were determined by comparing the elemental concentrations in the vitrinite concentrates to the concentrations in the companion whole coals. The ratios of these concentrations for 33 selected elements are shown in Figure 1. Ratios greater than 1 indicate organic affinity, and ratios less than 1 indicate inorganic affinity.
Br and W generally showed organic affinity in all samples in this study. In the nine samples from the eastern United States (Fig. 1A-C) less than one-fourth of the trace elements show organic affinity compared to nearly one-half for the three English and Australian samples (Fig. 1D). The elements that generally show organic affinity in the non-U.S.A. samples studied include As, Cs, Hf, and Ni, which have generally inorganic affinities in the U.S.A. samples, and Cr, Sb, Se, and U, which have mixed (both organic and inorganic) affinities, in the U.S.A. coals studied, has an inorganic affinity in the English coals studied. B shows organic affinity in the samples from the Illinois basin (Fig. 1C). For the samples studied, Ba shows organic affinity in the Appalachian basin bituminous coals (Fig. 1B), inorganic affinity in the Illinois basin coals, and overall mixed affinities. In all the samples studied, Cu, Mn, Na, Sr, Ta, V, and Zn show mixed affinities, and A1, Co, Eu, Fe, Ga, K, La, Mg, Sc, Si, Th, Ti, and Ub have generally inorganic affinity.
The isotopic ratios of H, O and C in water within the Long Valley caldera, California reflect input from sources external to the hydrothermal reservoir. A decrease in δD in precipitation of 0.5‰ km−1, from west to east across Long Valley, is caused by the introduction of less fractionated marine moisture through a low elevation embayment in the Sierra Nevada Mountain Range. Relative to seasonal fluctuations in precipitation (−158 to −35‰.), δD ranges in hot and cold surface and groundwaters are much less variable (−135 to −105‰.). Only winter and spring moisture, reflecting higher precipitation rates with lighter isotopic signatures, recharge the hydrological system. The hydrothermal fluids are mixtures of isotopically heavy recharge (δD = − 115‰, δ18O = − 15‰) derived from the Mammoth embayment, and isotopically lighter cold water (δD = −135‰, δ18O = −18‰). This cold water is not representative of current local recharge. The δ13C values for dissolved carbon in hot water are significantly heavier (− 7 to − 3‰) than in cold water (−18 to −10‰) denoting a separate hydrothermal origin. These δ13C values overlie the range generally attributed to magmatic degassing of CO2. However, δ13C values of metamorphosed Paleozoic basement carbonates surrounding Long Valley fall in a similar range, indicating that hydrothermal decarbonization reactions are a probable source of CO2. The δ13C and δ18O values of secondary travertime and vein calcite indicate respective fractionation with CO2 and H2O at temperatures approximating current hydrothermal conditions.
The Thornthwaite potential evapotranspiration model is well known and widely used, but has received some criticism as it is primarily based on air temperature to estimate potential evapotranspiration. Errors of the Thornthwaite model can be analyzed using adjusted pan evaporation as an index of potential evapotranspiration. An examination of ratios of adjusted pan evaporation to Thornthwaite potential evapotranspiration indicates that the ratios are highest in the winter and lowest during summer months. This trend suggests a parabolic pattern. In this study a parabolic function is used to adjust Thornthwaite estimates of potential evapotranspiration. Forty locations east of the Rocky Mountains are analyzed and indicate that a parabolic adjustment of Thornthwaite potential evapotranspiration estimates generally increases correlation with adjusted pan evaporation and decreases error by 20 to 70 percent.
","language":"English","publisher":"Taylor & Francis","doi":"10.1080/02723646.1989.10642376","issn":"02723646","usgsCitation":"McCabe, G.J., 1989, A parabolic function to modify Thornthwaite estimates of potential evapotranspiration for the eastern United States: Physical Geography, v. 10, no. 2, p. 176-189, https://doi.org/10.1080/02723646.1989.10642376.","productDescription":"14 p.","startPage":"176","endPage":"189","costCenters":[],"links":[{"id":223743,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"10","issue":"2","noUsgsAuthors":false,"publicationDate":"2013-05-15","publicationStatus":"PW","scienceBaseUri":"5059e4d1e4b0c8380cd46951","contributors":{"authors":[{"text":"McCabe, G. J. Jr.","contributorId":77551,"corporation":false,"usgs":true,"family":"McCabe","given":"G.","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":369886,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70044339,"text":"70044339 - 1989 - Constraints on the Anadarko Basin-Wichita uplift boundary interpreted from aeromagnetic data","interactions":[],"lastModifiedDate":"2013-03-03T18:33:56","indexId":"70044339","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"seriesNumber":"90","title":"Constraints on the Anadarko Basin-Wichita uplift boundary interpreted from aeromagnetic data","docAbstract":"Modeling and interpretation of aeromagnetic data across the transition between the Anadarko basin and the Wichita uplift in the vicinity of the scarp on the Meers fault (Fig. 1) constrains structural relationships and lithologic contrasts at this boundary. We digitized aeromagnetic data from the map based on a detailed survey flown in 1954 (U.S. Geological Survey, 1975). The flight lines for this survey were oriented east-west, spaced 0.25 mi apart, and flown 500 ft above the ground. The digitized data were gridded using a minimum-curvature gridding program (MINC; Webring, 1981) and plotted as a color-shaded relief map using an unpublished program written by M. W. Webring. The color-shaded relief map was shown in the Anadarko Basin Workshop poster session. Figure 2 is a generalized contour map made from the digitized data, using the unpublished program CONTOURS, written by R. H. Bracken, R. H. Godson, and M. W. Webring.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Anadarko Basin symposium, 1988 (Circular 90)","largerWorkSubtype":{"id":4,"text":"Other Government Series"},"language":"English","publisher":"Oklahoma Geological Survey","publisherLocation":"Norman, OK","collaboration":"Proceedings of a symposium held April 5-6, 1988, at Norman, Oklahoma; cosponsored by the Oklahoma Geological Survey and the U.S. Geological Survey","usgsCitation":"Jones-Cecil, M., and Crone, A.J., 1989, Constraints on the Anadarko Basin-Wichita uplift boundary interpreted from aeromagnetic data, chap. of Anadarko Basin symposium, 1988 (Circular 90), p. 228-232.","productDescription":"5 p.","startPage":"228","endPage":"232","costCenters":[],"links":[{"id":268691,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268690,"type":{"id":11,"text":"Document"},"url":"https://www.ogs.ou.edu/pubsscanned/Circulars/Circular90.pdf"}],"country":"United States","state":"Oklahoma","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0,33.62 ], [ -103.0,37.0 ], [ -94.43,37.0 ], [ -94.43,33.62 ], [ -103.0,33.62 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51347f03e4b0e1603e4fec40","contributors":{"authors":[{"text":"Jones-Cecil, Meridee","contributorId":68313,"corporation":false,"usgs":true,"family":"Jones-Cecil","given":"Meridee","email":"","affiliations":[],"preferred":false,"id":475318,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Crone, Anthony J. 0000-0002-3006-406X crone@usgs.gov","orcid":"https://orcid.org/0000-0002-3006-406X","contributorId":790,"corporation":false,"usgs":true,"family":"Crone","given":"Anthony","email":"crone@usgs.gov","middleInitial":"J.","affiliations":[{"id":300,"text":"Geologic Hazards Science Center","active":true,"usgs":true}],"preferred":true,"id":475317,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70044334,"text":"70044334 - 1989 - Quantitative petrographic analysis of Desmoinesian sandstones from Oklahoma","interactions":[],"lastModifiedDate":"2013-03-03T10:40:44","indexId":"70044334","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"seriesNumber":"90","title":"Quantitative petrographic analysis of Desmoinesian sandstones from Oklahoma","docAbstract":"Desmoinesian sandstones from the northern Oklahoma platform and the Anadarko, Arkoma, and Ardmore basins record a complex interaction between mid-Pennsylvanian source-area tectonism and cyclic sedimentation patterns associated with numerous transgressions and regressions. Framework-grain summaries for 50 thin sections from sandstones of the Krebs, Cabaniss, and Marmaton Groups and their surface and subsurface equivalents were subjected to multivariate statistical analyses to establish regional compositional trends for provenance analysis. R-mode cluster and correspondence analyses were used to determine the contributing effect (total variance) of key framework grains. Fragments of monocrystalline and polycrystalline quartz; potassium and plagioclase feldspar; chert; and metamorphic, limestone, and mudstone-sandstone rock fragments contribute most to the variation in the grain population. Q-mode cluster and correspondence analyses were used to identify four petrofacies and establish the range of compositional variation in Desmoinesian sandstones. Petrofacies I is rich in monocrystalline quartz (78-98%); mica and rock fragments are rare. Petrofacies II is also rich in monocrystalline quartz (60-84%) and averages 12% total rock fragments. Petrofacies III and IV are compositionally heterogeneous and contain variable percentages of monocrystalline and polycrystalline quartz, potassium feldspar, mica, chert, and metamorphic and sedimentary rock fragments. Quantitative analyses indicate that Desmoinesian sandstones were derived from sedimentary, igneous, and metamorphic source areas. Sandstones of petrofacies I and II occur mostly in the lower Desmoinesian and are widely distributed, although they are most abundant in eastern and central Oklahoma; sandstones of petrofacies III and IV are widely distributed and occur primarily in the middle and upper Desmoinesian. The range of compositional variation and the distribution of petrofacies are related to paleotectonics and basin development, sediment recycling, and varying depositional environments.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Anadarko Basin symposium, 1988 (Circular 90)","largerWorkSubtype":{"id":4,"text":"Other Government Series"},"language":"English","publisher":"Oklahoma Geological Survey","publisherLocation":"Norman, OK","collaboration":"Proceedings of a symposium held April 5-6, 1988, at Norman, Oklahoma; cosponsored by the Oklahoma Geological Survey and the U.S. Geological Survey","usgsCitation":"Dyman, T.S., 1989, Quantitative petrographic analysis of Desmoinesian sandstones from Oklahoma, chap. of Anadarko Basin symposium, 1988 (Circular 90), p. 162-175.","productDescription":"14 p.","startPage":"162","endPage":"175","costCenters":[],"links":[{"id":268681,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268680,"type":{"id":11,"text":"Document"},"url":"https://www.ogs.ou.edu/pubsscanned/Circulars/Circular90.pdf"}],"country":"United States","state":"Oklahoma","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0,33.62 ], [ -103.0,37.0 ], [ -94.43,37.0 ], [ -94.43,33.62 ], [ -103.0,33.62 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51347f0ae4b0e1603e4fec66","contributors":{"authors":[{"text":"Dyman, Thaddeus S.","contributorId":83971,"corporation":false,"usgs":true,"family":"Dyman","given":"Thaddeus","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":475306,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70044329,"text":"70044329 - 1989 - Structural evolution of the southeastern portion of the Anadarko Basin region","interactions":[],"lastModifiedDate":"2013-03-03T09:45:50","indexId":"70044329","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"seriesNumber":"90","title":"Structural evolution of the southeastern portion of the Anadarko Basin region","docAbstract":"Field investigations in the Lake Classen-Turner Falls, Oklahoma, area of the northern Arbuckle anticline, on the southeastern margin of the Anadarko basin, indicate that transpressional (oblique compressional) deformation of Late Pennsylvanian age dominated the structural development of this area. The Arbuckle anticline is detached along the NW -trending, SW -dipping, left-reverse Arbuckle fault and is thrust obliquely onto the margin of the Tishomingo block to the east. Paleostress analysis of slip lines on mesoscopic faults along the northeastern limb of the Arbuckle anticline, associated in style and geometry with oblique Arbuckle thrusting, indicates compression directed N. 35-60° E.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Anadarko Basin symposium, 1988 (Circular 90)","largerWorkSubtype":{"id":4,"text":"Other Government Series"},"language":"English","publisher":"Oklahoma Geological Survey","publisherLocation":"Norman, OK","collaboration":"Proceedings of a symposium held April 5-6, 1988, at Norman, Oklahoma; cosponsored by the Oklahoma Geological Survey and the U.S. Geological Survey","usgsCitation":"Perry, W.J., 1989, Structural evolution of the southeastern portion of the Anadarko Basin region, chap. of Anadarko Basin symposium, 1988 (Circular 90), p. 77-77.","productDescription":"1 p.","startPage":"77","endPage":"77","costCenters":[],"links":[{"id":268671,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268670,"type":{"id":11,"text":"Document"},"url":"https://www.ogs.ou.edu/pubsscanned/Circulars/Circular90.pdf"}],"country":"United States","state":"Oklahoma","otherGeospatial":"Anadarko Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -103.0,33.62 ], [ -103.0,37.0 ], [ -94.43,37.0 ], [ -94.43,33.62 ], [ -103.0,33.62 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51347f0ce4b0e1603e4fec72","contributors":{"authors":[{"text":"Perry, William J. Jr.","contributorId":32498,"corporation":false,"usgs":true,"family":"Perry","given":"William","suffix":"Jr.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":475299,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70044330,"text":"70044330 - 1989 - Horizontal stresses from well-bore breakouts and lithologies associated with their formation, Oklahoma and Texas Panhandle","interactions":[],"lastModifiedDate":"2013-03-03T10:00:00","indexId":"70044330","displayToPublicDate":"2013-01-01T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"seriesNumber":"90","title":"Horizontal stresses from well-bore breakouts and lithologies associated with their formation, Oklahoma and Texas Panhandle","docAbstract":"Orientations of crustal stresses are inferred from stress-induced well-bore breakouts in three areas in the south-central United States: the eastern part of the Anadarko basin in central Oklahoma, the Marietta basin in south-central Oklahoma, and the Bravo dome area of the central Texas Panhandle. Inferred directions of maximum horizontal principal stress (SHmax) are ENE for the eastern Anadarko basin, and NE for the Marietta basin and the Bravo dome area. For the Bravo dome area, the magnitudes of the three principal stresses (S1, S2, S3) are known from existing hydraulic-fracturing (hydrofrac) measurements, and a normal-faulting stress regime (SV > SHmax > SHmin) is implied. For the eastern Anadarko basin and the Marietta basin, the magnitudes of the principal stresses are not known. Because Quaternary left-lateral oblique slip on the Meers fault in south-central Oklahoma suggests strike-slip (SHmax > Sv > SHmin) and reverse faulting (SHmax > SHmin > SV), the study region is inferred to be a possible transition zone between areas of extensional and compressional stresses. Breakout data from the eastern Anadarko basin yield a single consistent SHmax orientation. Data from the Marietta basin and the Bravo dome area have bimodal-orthogonal distributions consisting of breakouts and orthogonal sets of well-bore enlargement orientations. Orthogonal trends in the data are probably related to drilling-induced hydraulic fracturing of the well bore, or to preexisting natural fractures or joint sets intersecting the well bore. On the dipmeter log, breakouts and fracture enlargements have elliptical cross sections of similar size and shape. Orthogonally oriented well-bore enlargements are differentiated by comparing their long-axis orientations with directions of known or inferred horizontal stress. Dispersion, or data scatter, among enlargement orientations (bimodal data sets) increases the standard deviations for many well data sets from the Marietta basin and the Bravo dome area. In these two areas, some dispersion may reflect variation in stress conditions across fault-bounded blocks and the orientations of fractures or joints within these blocks. Although breakouts and fracture enlargements formed in all parts of the thick sequences of sedimentary rocks logged, they occurred primarily in limestone, shale, and dolomitic rocks, reflecting the abundance of these rock types in the study areas.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Anadarko Basin symposium, 1988 (Circular 90)","largerWorkSubtype":{"id":4,"text":"Other Government Series"},"language":"English","publisher":"Oklahoma Geological Survey","publisherLocation":"Norman, OK","collaboration":"Proceedings of a symposium held April 5-6, 1988, at Norman, Oklahoma; cosponsored by the Oklahoma Geological Survey and the U.S. Geological Survey","usgsCitation":"Dart, R.L., 1989, Horizontal stresses from well-bore breakouts and lithologies associated with their formation, Oklahoma and Texas Panhandle, chap. of Anadarko Basin symposium, 1988 (Circular 90), p. 97-120.","productDescription":"24 p.","startPage":"97","endPage":"120","costCenters":[],"links":[{"id":268673,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":268672,"type":{"id":11,"text":"Document"},"url":"https://www.ogs.ou.edu/pubsscanned/Circulars/Circular90.pdf"}],"country":"United States","state":"Oklahoma;Texas","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -104.0,33.0 ], [ -104.0,38.0 ], [ -94.0,38.0 ], [ -94.0,33.0 ], [ -104.0,33.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"51347f07e4b0e1603e4fec54","contributors":{"authors":[{"text":"Dart, Richard L. dart@usgs.gov","contributorId":1209,"corporation":false,"usgs":true,"family":"Dart","given":"Richard","email":"dart@usgs.gov","middleInitial":"L.","affiliations":[],"preferred":true,"id":475300,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70038761,"text":"70038761 - 1989 - Borax in the supraglacial moraine of the Lewis Cliff, Buckley Island quadrangle--first Antarctic occurrence","interactions":[],"lastModifiedDate":"2012-06-20T01:01:36","indexId":"70038761","displayToPublicDate":"2012-01-01T15:23:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":812,"text":"Antarctic Journal of the United States","active":true,"publicationSubtype":{"id":10}},"title":"Borax in the supraglacial moraine of the Lewis Cliff, Buckley Island quadrangle--first Antarctic occurrence","docAbstract":"During the 1987-1988 austral summer field season, membersof the south party of the antarctic search for meteorites south-ern team* working in the Lewis Cliff/Colbert Hills region dis-covered several areas of unusual mineralization within theLewis Cliff ice tongue and its associated moraine field (figure1). The Lewis Cliff ice tongue (84°15'S 161°25'E) is a meteorite-stranding surface of ablating blue ice, about 2.3 by 7.0 kilo-meters, bounded on the west by the Lewis Cliff, on the northand northeast by a large supraglacial moraine, and on the eastby the Colbert Hills. To the south it opens to the Walcott Névé.Because it is a meteorite-stranding surface, the major component of ice motion in the area is believed to be vertical(Whillans and Cassidy 1983). The presence of Thule-Baffinmoraines at the northern terminus of the blue ice tends tosupport the hypothesis that the area underlying the moraineis essentially stagnant and that ice arriving from the south ispiling up against it. Areas containing mineral deposits werefound within the moraine field to the north and east of theblue ice margin and also along the east margins of the blue iceitself. Subsequent X-ray diffraction analyses of these depositshave shown that they are composed predominantly of nah-colite (NaHCO3), trona [Na3(CO3)(HCO3) · 2H20], borax[Na2B405(OH)4 · 8H20], and a new hexagonal hydrous sulfatespecies. This paper reports the details of the borax occurrence,because it is the first known on the continent.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Antarctic Journal of the United States","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"National Science Foundation, Office of Polar Programs","publisherLocation":"Washington, D.C.","usgsCitation":"Fitzpatrick, J.J., and Muhs, D., 1989, Borax in the supraglacial moraine of the Lewis Cliff, Buckley Island quadrangle--first Antarctic occurrence: Antarctic Journal of the United States, v. 24, no. 5, p. 63-65.","productDescription":"3 p.","startPage":"63","endPage":"65","costCenters":[{"id":308,"text":"Geology and Environmental Change Science Center","active":false,"usgs":true}],"links":[{"id":257720,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":257696,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://s3.amazonaws.com/Antarctica/AJUS/AJUSvXXIVn5/AJUSvXXIVn5p63.pdf","linkFileType":{"id":1,"text":"pdf"}}],"otherGeospatial":"Lewis Cliff;Buckley Island;Antarctica","volume":"24","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f211e4b0c8380cd4afbc","contributors":{"authors":[{"text":"Fitzpatrick, J. J.","contributorId":95078,"corporation":false,"usgs":true,"family":"Fitzpatrick","given":"J.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":464883,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Muhs, D.R. 0000-0001-7449-251X","orcid":"https://orcid.org/0000-0001-7449-251X","contributorId":61460,"corporation":false,"usgs":true,"family":"Muhs","given":"D.R.","affiliations":[],"preferred":false,"id":464882,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70016442,"text":"70016442 - 1989 - The style of late Cenozoic deformation at the eastern front of the California Coast Ranges","interactions":[],"lastModifiedDate":"2025-09-09T16:20:02.592969","indexId":"70016442","displayToPublicDate":"2010-07-26T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3524,"text":"Tectonics","active":true,"publicationSubtype":{"id":10}},"title":"The style of late Cenozoic deformation at the eastern front of the California Coast Ranges","docAbstract":"The 1983 Coalinga earthquake occurred at the eastern boundary of the California Coast Ranges in response to northeast directed thrusting. Such movements over the past 2 Ma have produced Coalinga anticline by folding above the blind eastern tip of the Coalinga thrust zone. The 600-km length of the Coast Ranges boundary shares a common structural setting that involves westward upturn of Cenozoic and Cretaceous strata at the eastern front of the Coast Ranges and a major, southwest facing step in the basement surface beneath the western Great Valley. Like Coalinga anticline, Pliocene and Quaternary folding and faulting along the rest of the boundary also result from northeast–southwest compression acting nearly perpendicular to the strike of the San Andreas fault. We suggest that much of this deformation is related to active thrusts beneath the eastern Coast Ranges. The step in the basement surface beneath the Great Valley seems to have controlled the distribution of this deformation and the shape of the Coast Ranges boundary.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TC008i002p00237","issn":"02787407","usgsCitation":"Wentworth, C.M., and Zoback, M.D., 1989, The style of late Cenozoic deformation at the eastern front of the California Coast Ranges: Tectonics, v. 8, no. 2, p. 237-246, https://doi.org/10.1029/TC008i002p00237.","productDescription":"10 p.","startPage":"237","endPage":"246","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":223023,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -124.32227407395877,\n 41.97832769849734\n ],\n [\n -124.74825712118408,\n 40.481762804899304\n ],\n [\n -123.95784846843993,\n 37.723480083156964\n ],\n [\n -120.98130768802946,\n 33.960324024322546\n ],\n [\n -117.91076108785359,\n 32.52389178858395\n ],\n [\n -114.47724181066988,\n 32.56556837931663\n ],\n [\n -114.0284147380225,\n 34.84897918676069\n ],\n [\n -120.04211889323415,\n 39.2058471835924\n ],\n [\n -119.7547739371154,\n 41.9554707528047\n ],\n [\n -124.32227407395877,\n 41.97832769849734\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"8","issue":"2","noUsgsAuthors":false,"publicationDate":"2010-07-26","publicationStatus":"PW","scienceBaseUri":"505bb0a2e4b08c986b324fa8","contributors":{"authors":[{"text":"Wentworth, Carl M. 0000-0003-2569-569X cwent@usgs.gov","orcid":"https://orcid.org/0000-0003-2569-569X","contributorId":1178,"corporation":false,"usgs":true,"family":"Wentworth","given":"Carl","email":"cwent@usgs.gov","middleInitial":"M.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":373550,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zoback, Mark D.","contributorId":80275,"corporation":false,"usgs":true,"family":"Zoback","given":"Mark","middleInitial":"D.","affiliations":[],"preferred":false,"id":373549,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70015407,"text":"70015407 - 1989 - Taconic plate kinematics as revealed by foredeep stratigraphy, Appalachian orogen","interactions":[],"lastModifiedDate":"2025-09-09T16:53:48.049201","indexId":"70015407","displayToPublicDate":"2010-07-26T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3524,"text":"Tectonics","active":true,"publicationSubtype":{"id":10}},"title":"Taconic plate kinematics as revealed by foredeep stratigraphy, Appalachian orogen","docAbstract":"Destruction of the Ordovician passive margin of eastern North America is recorded by an upward deepening succession of carbonates, shales, and flysch. A compilation of the age of shelf drowning (carbonate-to-shale transition) reveals the degree to which orogeny was diachronous both across and along strike. Shelf drowning occurred first at the northern end of the orogen in Newfoundland, then at the southern end of the orogen in Georgia, and finally in Quebec. Diachronism is attributed to oblique collision between an irregular passive margin, that had a deep embayment in Quebec, and at least one east dipping subduction complex. The rate of plate convergence during collision is estimated at 1 to 2 cm/yr, and the minimum width of the ocean that closed is estimated at 500 to 900 km. Far-traveled deepwater sequences in the thrust belt contain anomalously old Taconic flysch, related to early arrival of the continental slope/rise at a west advancing trench then located far to the east. The drowning isochron map provides a new basis for estimating tectonic transport distances of four of these allochthons (about 165 to 450 km), results not readily obtained by conventional structural analysis.
","language":"English","publisher":"American Geophysical Union","doi":"10.1029/TC008i005p01037","issn":"02787407","usgsCitation":"Bradley, D.C., 1989, Taconic plate kinematics as revealed by foredeep stratigraphy, Appalachian orogen: Tectonics, v. 8, no. 5, p. 1037-1049, https://doi.org/10.1029/TC008i005p01037.","productDescription":"13 p.","startPage":"1037","endPage":"1049","costCenters":[],"links":[{"id":224307,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","otherGeospatial":"Appalachian Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -59.94794184613204,\n 53.783005810210994\n ],\n [\n -66.52193972184966,\n 49.42391661877889\n ],\n [\n -84.05589482730278,\n 32.29826164743447\n ],\n [\n -82.25406401000738,\n 31.27460409801749\n ],\n [\n -72.41174206402178,\n 42.00001551829209\n ],\n [\n -60.01457676108012,\n 51.99456174559443\n ],\n [\n -59.94794184613204,\n 53.783005810210994\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"8","issue":"5","noUsgsAuthors":false,"publicationDate":"2010-07-26","publicationStatus":"PW","scienceBaseUri":"505ba3ace4b08c986b31fdee","contributors":{"authors":[{"text":"Bradley, D. C.","contributorId":17634,"corporation":false,"usgs":true,"family":"Bradley","given":"D.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":370869,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5222251,"text":"5222251 - 1989 - Avian community response to small-scale habitat disturbance in Maine","interactions":[],"lastModifiedDate":"2023-11-16T12:21:24.686702","indexId":"5222251","displayToPublicDate":"2010-06-16T12:19:09","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1176,"text":"Canadian Journal of Zoology","active":true,"publicationSubtype":{"id":10}},"title":"Avian community response to small-scale habitat disturbance in Maine","docAbstract":"The effects of small clearcuts (1 - 8 ha) on avian communities in the forest of eastern Maine were studied using point counts during spring 1978 - 1981. Surveys were conducted in uncut (control) and clear-cut (treatment) plots in three stand types: conifer, hardwood, and mixed growth. We used a mark-recapture model and its associated jackknife species richness estimator (N), as an indicator of avian community structure. Increases in estimated richness (N) and Shannon - Weaver diversity (H') were noted in the treated hardwood and mixed growth, but not in the conifer stands. Seventeen avian species increased in relative abundance, whereas two species declined. Stand treatment was associated with important changes in bird species composition. Increased habitat patchiness and the creation of forest edge are hypothesized as causes for the greater estimates of richness and diversity.","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/z89-057","usgsCitation":"Derleth, E., McAuley, D., and Dwyer, T., 1989, Avian community response to small-scale habitat disturbance in Maine: Canadian Journal of Zoology, v. 67, no. 2, p. 385-390, https://doi.org/10.1139/z89-057.","productDescription":"6 p.","startPage":"385","endPage":"390","numberOfPages":"6","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":194131,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"67","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a82e4b07f02db64afb8","contributors":{"authors":[{"text":"Derleth, E.L.","contributorId":31483,"corporation":false,"usgs":true,"family":"Derleth","given":"E.L.","affiliations":[],"preferred":false,"id":335914,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McAuley, D.G. 0000-0003-3674-6392","orcid":"https://orcid.org/0000-0003-3674-6392","contributorId":15296,"corporation":false,"usgs":true,"family":"McAuley","given":"D.G.","affiliations":[],"preferred":false,"id":335913,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dwyer, T.J.","contributorId":56177,"corporation":false,"usgs":true,"family":"Dwyer","given":"T.J.","email":"","affiliations":[],"preferred":false,"id":335915,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":5222576,"text":"5222576 - 1989 - Population ecology and harvest of the American black duck: a review","interactions":[],"lastModifiedDate":"2012-03-02T17:16:07","indexId":"5222576","displayToPublicDate":"2010-06-16T12:19:06","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3779,"text":"Wildlife Society Bulletin","onlineIssn":"1938-5463","printIssn":"0091-7648","active":true,"publicationSubtype":{"id":10}},"title":"Population ecology and harvest of the American black duck: a review","docAbstract":"1. The purpose of our review was to examine available data on population trends and current status of black ducks and trends in natality and survival and to relate these, where possible, to changes in habitat, predation, disease, contaminants, harvest, and hybridization with mallards. 2. The number of black ducks tallied in the winter survey has declined steadily over the past 30 years at an average rate of about 3%/ year. Reliability and precision of the survey are uncertain; it may not provide an adequate index to the continental population of black ducks. Breeding surveys are incomplete and sporadic, but black ducks have decreased in Ontario and increased in the Maritime Provinces and Quebec. 3. Recent declines in numbers of black ducks tallied in the winter survey are not unusual in magnitude or much different from those that have occurred among several other species of waterfowl. 4. At present, black ducks are not especially scarce relative to numbers of several other ducks in eastern North America. 5. There is no solid evidence of major decreases in quality or quantity of breeding habitat for black ducks in recent years; in some areas, habitat has improved. 6. Natural mortality of black ducks has not been well studied, but does not seem unusually high compared to other dabbling ducks. 7. Harvest rates of black ducks are similar to those of sympatric mallards as determined by banding analyses. 8. There is no strong evidence for direct effects of contaminants on black ducks, but some indirect effects through invertebrate food resources have been detected. 9. Age ratios in black ducks show no trend in the past 18 years. 10. The quality and quantity of wintering habitat for black ducks have decreased substantially in some areas. 11. Disease and other natural mortality that affect black ducks do .not occur in unusually high frequency. 12. A decline in harvest of black ducks has occurred; most of the decline has been in the United States, especially since restrictive regulations were implemented in 1983. 13. Recovery rates of black ducks have declined recently in the U.S., but not in Canada. 14. Survival rates of black ducks are 56-63% for adults and 43% for young. These rates of survival are similar to comparable estimates in sympatric mallards. 15. Long hunting seasons may depress survival in some sex-age classes of black ducks, buteffects of small reductions in survival on population trends are unknown. 16. Available evidence does not support the contention that hunting is either the sole or most important cause of the decline in the winter tally of black duck numbers. 17. Surveys and banding of black ducks should be thoroughly reviewed and maintained or improved as warranted. Obtaining or maintaining a reasonable index to numbers of black ducks is the top priority among survey needs. 18. Experimental manipulation of hunting seasons should be considered to elucidate relationships among regulations, harvest, survival, and population trends. 19. Black ducks and mallards are genetically similar; there is as much genetic differentiation within the 2 species as there is between them. 20. Black duck x mallard hybrids are fertile. Hybrids are difficult to detect by plumage and thus published frequencies (0-13%) of hybrids may be low. 21. Hybridization could be a result of concomitant mallard increases and black duck decreases, or changes in black duck-to-mallard ratios could be from hybridization and genetic swamping of black ducks.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Wildlife Society Bulletin","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"Rusch, D., Ankney, C., Boyd, H., Longcore, J.R., Montalbano, F., Ringelman, J., and Stotts, V.D., 1989, Population ecology and harvest of the American black duck: a review: Wildlife Society Bulletin, v. 17, no. 4, p. 379-406.","productDescription":"379-406","startPage":"379","endPage":"406","numberOfPages":"28","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":194197,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":17904,"rank":200,"type":{"id":11,"text":"Document"},"url":"https://www.jstor.org/stable/3782702","linkFileType":{"id":5,"text":"html"}}],"volume":"17","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db684010","contributors":{"authors":[{"text":"Rusch, D. H.","contributorId":19897,"corporation":false,"usgs":true,"family":"Rusch","given":"D. H.","affiliations":[],"preferred":false,"id":336555,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ankney, C.D.","contributorId":48904,"corporation":false,"usgs":true,"family":"Ankney","given":"C.D.","email":"","affiliations":[],"preferred":false,"id":336557,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Boyd, H.","contributorId":65942,"corporation":false,"usgs":true,"family":"Boyd","given":"H.","email":"","affiliations":[],"preferred":false,"id":336559,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Longcore, J. R. 0000-0003-4898-5438","orcid":"https://orcid.org/0000-0003-4898-5438","contributorId":43835,"corporation":false,"usgs":true,"family":"Longcore","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":336556,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Montalbano, Frank III","contributorId":86715,"corporation":false,"usgs":true,"family":"Montalbano","given":"Frank","suffix":"III","email":"","affiliations":[],"preferred":false,"id":336560,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Ringelman, J.K.","contributorId":65418,"corporation":false,"usgs":true,"family":"Ringelman","given":"J.K.","email":"","affiliations":[],"preferred":false,"id":336558,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Stotts, Vernon D.","contributorId":86724,"corporation":false,"usgs":false,"family":"Stotts","given":"Vernon","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":336561,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":5222298,"text":"5222298 - 1989 - Population declines in North American birds that migrate to the neotropics","interactions":[],"lastModifiedDate":"2012-02-02T00:14:36","indexId":"5222298","displayToPublicDate":"2010-06-16T12:19:06","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3164,"text":"Proceedings of the National Academy of Sciences","active":true,"publicationSubtype":{"id":10}},"title":"Population declines in North American birds that migrate to the neotropics","docAbstract":"Using data from the North American Breeding Bird Survey, we determined that most neotropical migrant bird species that breed in forests of the eastern United States and Canada have recently (1978-1987) declined in abundance after a period of stable or increasing populations. Most permanent residents and temperate-zone migrants did not show a general pattern of decrease during this period. Field data from Mexico were used to classify a subset of the neotropical migrants as using forest or scrub habitats during winter. Population declines during 1978-1987 were significantly greater among the forest-wintering species, while populations of scrub-wintering species increased. The same subset of neotropical migrants also showed overall declines in forest-breeding species, but no significant differences existed between species breeding in forest and scrub habitats. Neotropical migrant species that primarily use forested habitats in either wintering or breeding areas are declining, but a statistically significant association between habitat and population declines was detected only in the tropics.","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Proceedings of the National Academy of Sciences","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","collaboration":"3808_Robbins.pdf","usgsCitation":"Robbins, C., Sauer, J., Greenberg, R., and Droege, S., 1989, Population declines in North American birds that migrate to the neotropics: Proceedings of the National Academy of Sciences, v. 86, no. 19, p. 7658-7662.","productDescription":"7658-7662","startPage":"7658","endPage":"7662","numberOfPages":"5","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":94268,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://www.pnas.org/content/86/19/7658.abstract","linkFileType":{"id":5,"text":"html"}},{"id":17903,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://www.pubmedcentral.nih.gov/picrender.fcgi?artid=298126&blobtype=pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":193697,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"86","issue":"19","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad6e4b07f02db68430a","contributors":{"authors":[{"text":"Robbins, C.S.","contributorId":53907,"corporation":false,"usgs":true,"family":"Robbins","given":"C.S.","email":"","affiliations":[],"preferred":false,"id":336016,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sauer, J.R. 0000-0002-4557-3019","orcid":"https://orcid.org/0000-0002-4557-3019","contributorId":66197,"corporation":false,"usgs":true,"family":"Sauer","given":"J.R.","affiliations":[],"preferred":false,"id":336018,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Greenberg, R.S.","contributorId":27158,"corporation":false,"usgs":true,"family":"Greenberg","given":"R.S.","email":"","affiliations":[],"preferred":false,"id":336015,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Droege, Sam 0000-0003-4393-0403","orcid":"https://orcid.org/0000-0003-4393-0403","contributorId":64185,"corporation":false,"usgs":true,"family":"Droege","given":"Sam","affiliations":[{"id":50464,"text":"Eastern Ecological Science Center","active":true,"usgs":true}],"preferred":false,"id":336017,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70015525,"text":"70015525 - 1989 - Lower Permian sediment-gravity-flow sequence, eastern California","interactions":[],"lastModifiedDate":"2025-07-23T15:35:30.98844","indexId":"70015525","displayToPublicDate":"2003-04-11T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3368,"text":"Sedimentary Geology","active":true,"publicationSubtype":{"id":10}},"title":"Lower Permian sediment-gravity-flow sequence, eastern California","docAbstract":"The Lower Permian (middle Wolfcampian) Zinc Hill sequence, a 65- to 110-m-thick series of beds in the Owens Valley Group in east-central California, comprises sediment-gravity-flow deposits consisting of carbonate sediment that originated on, and siliciclastic sediment that may have been generally ponded behind, a carbonate shelf to the east and northeast. Thickness patterns and paleocurrent indicators show that the sediment forming this sequence was transported primarily southeastward and deposited in a southeast-trending, lobe-shaped body. Evidently, the sediment was carried from the shelf by sediment-gravity flows that travelled westward down the slope and then turned southeastward upon reaching a southeast-trending basin at the base of the slope. Data derived from the study of this basin, which paralleled the shelf edge and is thought to have formed parallel to a southeast-oriented segment of the Early Permian continental margin, constitute one of the most important arguments favoring a Pennsylvanian to Early Permian age of truncation of the western North American continental margin.
","language":"English","publisher":"Elsevier","doi":"10.1016/0037-0738(89)90080-8","issn":"00370738","usgsCitation":"Stevens, C., Lico, M.S., and Stone, P., 1989, Lower Permian sediment-gravity-flow sequence, eastern California: Sedimentary Geology, v. 64, no. 1-3, p. 1-12, https://doi.org/10.1016/0037-0738(89)90080-8.","productDescription":"12 p.","startPage":"1","endPage":"12","costCenters":[],"links":[{"id":223721,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"eastern California","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.25036992550474,\n 36.24083341099646\n ],\n [\n -116.25036992550474,\n 35.348277037935134\n ],\n [\n -114.89567591529288,\n 35.348277037935134\n ],\n [\n -114.89567591529288,\n 36.24083341099646\n ],\n [\n -116.25036992550474,\n 36.24083341099646\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"64","issue":"1-3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a4a72e4b0c8380cd68d88","contributors":{"authors":[{"text":"Stevens, C.H.","contributorId":16102,"corporation":false,"usgs":true,"family":"Stevens","given":"C.H.","affiliations":[],"preferred":false,"id":371152,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lico, Michael S.","contributorId":75897,"corporation":false,"usgs":true,"family":"Lico","given":"Michael","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":371153,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Stone, Paul 0000-0002-1439-0156 pastone@usgs.gov","orcid":"https://orcid.org/0000-0002-1439-0156","contributorId":273,"corporation":false,"usgs":true,"family":"Stone","given":"Paul","email":"pastone@usgs.gov","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":371154,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70015231,"text":"70015231 - 1989 - Tulelake, California: The last 3 million years","interactions":[],"lastModifiedDate":"2025-06-10T16:00:28.838301","indexId":"70015231","displayToPublicDate":"2003-04-02T00:00:00","publicationYear":"1989","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2996,"text":"Palaeogeography, Palaeoclimatology, Palaeoecology","printIssn":"0031-0182","active":true,"publicationSubtype":{"id":10}},"title":"Tulelake, California: The last 3 million years","docAbstract":"The Tulelake basin, formed by east-west extension and faulting during the past several million years, contains at least 550 m of lacustrine sediment. Interdisciplinary studies of a 334 m-long cored section from the town of Tulelake, California, near the center of the basin, document a 3-m.y. record of environmental changes. The core consists of a thick sequence of diatomaceous clayey, silty, and marly lacustrine sediments interbedded with numerous tephra layers. Paleomagnetic study puts the base of the core at about 3.0 Ma. Twelve widespread silicic tephra units provide correlations with other areas and complement age control provided by magnetostratigraphy; mafic and silicic tephra units erupted from local sources are also common in the core. Widespread tephra units include the Llao Rock pumice (=Tsoyawata, 7 ka), the Trego Hot Springs Bed (23 ka), and the Rockland (0.40 Ma), Lava Creek (0.62 Ma), and Rio Dell (1.5 Ma) ash beds, as well as several ash beds also found at Summer Lake, Oregon, and an ash bed originally recognized in DSDP hole 173 in the northeastern Pacific. Several tephra layers found in the core also occur in lacustrine beds exposed around the margins of the basin and elsewhere in the ancestral lacustrine system.
Diatoms are present throughout the section. Pollen is present in most of the section, but some barren zones are found in the interval between 50 and 140 m; the greatest change in behavior of the pollen record takes place just above the top of the Olduvai Normal-Polarity Subchronozone. Ostracodes are present only in high-carbonate (>10% CaCO3) intervals. Evolutionary changes are found in the diatom and ostracode records. Bulk geochemical analyses show significant changes in elemental composition of the sediment through time.
","language":"English","publisher":"Elsevier","doi":"10.1016/0031-0182(89)90134-X","issn":"00310182","usgsCitation":"Adam, D., Sarna-Wojcicki, A., Rieck, H.J., Bradbury, J., Dean, W., and Forester, R.M., 1989, Tulelake, California: The last 3 million years: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 72, p. 89-103, https://doi.org/10.1016/0031-0182(89)90134-X.","productDescription":"15 p.","startPage":"89","endPage":"103","costCenters":[],"links":[{"id":224141,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Tulelake","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.590433212109,\n 42.001532888963766\n ],\n [\n -121.590433212109,\n 41.82182577352725\n ],\n [\n -121.39683255075273,\n 41.82182577352725\n ],\n [\n -121.39683255075273,\n 42.001532888963766\n ],\n [\n -121.590433212109,\n 42.001532888963766\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"72","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb8bae4b08c986b327a2b","contributors":{"authors":[{"text":"Adam, D.P.","contributorId":14815,"corporation":false,"usgs":true,"family":"Adam","given":"D.P.","email":"","affiliations":[],"preferred":false,"id":370390,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sarna-Wojcicki, A.M. 0000-0002-0244-9149","orcid":"https://orcid.org/0000-0002-0244-9149","contributorId":104022,"corporation":false,"usgs":true,"family":"Sarna-Wojcicki","given":"A.M.","affiliations":[],"preferred":false,"id":370394,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Rieck, Hugh J.","contributorId":44560,"corporation":false,"usgs":true,"family":"Rieck","given":"Hugh","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":370391,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bradbury, J.P.","contributorId":14431,"corporation":false,"usgs":true,"family":"Bradbury","given":"J.P.","email":"","affiliations":[],"preferred":false,"id":370389,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Dean, W.E.","contributorId":97099,"corporation":false,"usgs":true,"family":"Dean","given":"W.E.","email":"","affiliations":[],"preferred":false,"id":370393,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Forester, R. M.","contributorId":76332,"corporation":false,"usgs":true,"family":"Forester","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":370392,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}} ]}