Montmorillonite was found to be the dominant clay mineral in surface horizons of certain soils of the North Carolina Coastal Plain whereas a 2:1-2:2 intergrade clay mineral was dominant in subjacent horizons. In all soils where this clay mineral sequence was found, the surface horizon was low in pH (below 4⋅5) and high in organic matter content. In contrast, data from studies of other soils of this region (Weed and Nelson, 1962) show that: (1) montmorillonite occurs infrequently; (2) maximum accumulation of the 2:1-2:2 intergrade normally occurs in the surface horizon and decreases with depth in the profile; (3) organic matter contents are low; and (4) pH values are only moderately acid (pH 5-6).
It is theorized that the montmorillonite in the surface horizon of the soils studied originated by pedogenic weathering of the 2:1-2:2 intergrade clay mineral. The combined effects of low pH (below 4⋅5) and high organic matter content in surface horizons are believed to be the agents responsible for this mineral transformation. The protonation and solubilization (reverse of hydrolysis) of Al-polymers in the interlayer of expansible clay minerals will occur at or below pH 4⋅5 depending on the charge and steric effects of the interlayer. A low pH alone may cause this solubilization and thus mineral transformation, but in the soils studied the organic matter is believed to facilitate and accelerage the transformation. The intermediates of organic matter decomposition provide an acid environment, a source of protons, and a source of watersoluble mobile organic substances (principally fulvic acids) which have the ability to complex the solubilized aluminum and move it down the profile. This continuous removal of solubilized aluminum would provide for a favorable gradient for aluminum solubilization.
The drainage class or position in a catena is believed to be less important than the chemical factors in formation of montmorillonite from 2:1-2:2 intergrade, because montmorillonite is present in all drainage classes if the surface horizon is low in pH and high in organic matter.
","language":"English","publisher":"The Clay Minerals Society","doi":"10.1346/CCMN.1969.0160602","usgsCitation":"Malcolm, R., Nettleton, W., and McCracken, R.J., 1968, Pedogenic formation of montmorillonite from a 2:1-2:2 intergrade clay mineral: Clays and Clay Minerals, v. 16, no. 6, p. 405-414, https://doi.org/10.1346/CCMN.1969.0160602.","productDescription":"10 p.","startPage":"405","endPage":"414","costCenters":[],"links":[{"id":221111,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"16","issue":"6","noUsgsAuthors":false,"publicationDate":"2024-07-01","publicationStatus":"PW","scienceBaseUri":"505a7629e4b0c8380cd77f6e","contributors":{"authors":[{"text":"Malcolm, Ronald L.","contributorId":46075,"corporation":false,"usgs":true,"family":"Malcolm","given":"Ronald L.","affiliations":[],"preferred":false,"id":361073,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nettleton, W.D.","contributorId":91988,"corporation":false,"usgs":true,"family":"Nettleton","given":"W.D.","email":"","affiliations":[],"preferred":false,"id":361074,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McCracken, R. J.","contributorId":102205,"corporation":false,"usgs":false,"family":"McCracken","given":"R.","middleInitial":"J.","affiliations":[],"preferred":false,"id":361075,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":35209,"text":"b1251H - 1968 - Geology of the Magruder Mountain area, Nevada-California","interactions":[],"lastModifiedDate":"2023-03-09T21:38:51.204426","indexId":"b1251H","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1251","chapter":"H","title":"Geology of the Magruder Mountain area, Nevada-California","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1251H","usgsCitation":"McKee, E.H., 1968, Geology of the Magruder Mountain area, Nevada-California: U.S. Geological Survey Bulletin 1251, Report: iv, 40 p.; 1 Plate: 29.00 x 19.50 inches, https://doi.org/10.3133/b1251H.","productDescription":"Report: iv, 40 p.; 1 Plate: 29.00 x 19.50 inches","costCenters":[],"links":[{"id":413928,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_21333.htm","linkFileType":{"id":5,"text":"html"}},{"id":63082,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1251h/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":63081,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1251h/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":166130,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1251h/report-thumb.jpg"}],"country":"United States","state":"Pennsylvania","otherGeospatial":"McCalls Ferry-Quarryville district","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -76.5,\n 40\n ],\n [\n -76.5,\n 39.75\n ],\n [\n -76,\n 39.75\n ],\n [\n -76,\n 40\n ],\n [\n -76.5,\n 40\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67ea4d","contributors":{"authors":[{"text":"McKee, Edwin H. mckee@usgs.gov","contributorId":3728,"corporation":false,"usgs":true,"family":"McKee","given":"Edwin","email":"mckee@usgs.gov","middleInitial":"H.","affiliations":[],"preferred":true,"id":214254,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70209107,"text":"70209107 - 1968 - Seismic evidence for the thickness of Cenozoic deposits in Mono Basin, California","interactions":[],"lastModifiedDate":"2020-03-16T17:32:43","indexId":"70209107","displayToPublicDate":"1968-12-31T17:27:29","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5935,"text":"Bulletin of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Seismic evidence for the thickness of Cenozoic deposits in Mono Basin, California","docAbstract":"From gravity and limited seismic data obtained in 1957, Pakiser and others (1960) reported a thickness of Cenozoic deposits in the deepest part of Mono Basin, California, of 5.5 ± 1.5 km. Later, in 1962, from a series of chemical explosions in the westernmost part of Mono Basin and outside the limits of the main depressed structure, the thickness of Cenozoic deposits was estimated to be 1.6 km. In 1966, a series of ten 1-ton chemical explosions was detonated in Mono Lake near the deepest part of the Mono Basin structure for the purpose of studying the relative effectiveness of different types of explosives in generating seismic energy. Seismic waves recorded at distances 25.0 to 92.3 km from the explosions were delayed by 1.43 seconds (referred to a shot on bedrock) as they descended through the low-velocity Cenozoic deposits of Mono Basin. By using the velocities of Cenozoic deposits as determined during the 1957 field season, the thickness of Cenozoic deposits required to account for the 1.43-second delay determined in 1966 has been estimated to be about 5 ± 1 km. The delay of seismic waves emerging in Long Valley was less than expected, indicating that they were propagated into Long Valley mainly through high-velocity rocks. From the rate of deposition of Cenozoic rocks in Mono Basin based on the age and depth of burial of the Bishop Tuff, it was estimated that Mono Basin began to subside in early or middle Pliocene time.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1833:SEFTTO]2.0.CO;2","usgsCitation":"Pakiser, L.C., 1968, Seismic evidence for the thickness of Cenozoic deposits in Mono Basin, California: Bulletin of the Geological Society of America, v. 79, no. 12, p. 1833-1838, https://doi.org/10.1130/0016-7606(1968)79[1833:SEFTTO]2.0.CO;2.","productDescription":"6 p.","startPage":"1833","endPage":"1838","costCenters":[],"links":[{"id":373305,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Mono Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.9647674560547,\n 37.8813571797486\n ],\n [\n -118.80546569824217,\n 37.8813571797486\n ],\n [\n -118.80546569824217,\n 37.98642201062662\n ],\n [\n -118.9647674560547,\n 37.98642201062662\n ],\n [\n -118.9647674560547,\n 37.8813571797486\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"79","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Pakiser, L. C.","contributorId":83512,"corporation":false,"usgs":true,"family":"Pakiser","given":"L.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":784956,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70209018,"text":"70209018 - 1968 - Borax solution at Kramer, California","interactions":[],"lastModifiedDate":"2020-03-11T17:28:45","indexId":"70209018","displayToPublicDate":"1968-12-31T17:23:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Borax solution at Kramer, California","docAbstract":"Material of obscure structure that forms part of the hanging wall of the great sodium borate ore body at Kramer, Kern County, Calif., is interpreted herein as collapsed insoluble claystone layers left where interbedded borax has been dissolved. Nodular ulexite in such collapsed material is secondary; relationships between primary borax and contemporaneous ulexite or other syngenetic borate minerals remain unestablished. The effects of solution also leave unestablished the original limits of borax deposition. It is suggested that collapsed claystone layers containing ulexite might be used as an indicator of proximity to borax elsewhere in the district.
","language":"English","publisher":"Society of Economic Geologist ","doi":"10.2113/gsecongeo.63.8.877","usgsCitation":"Smith, W.C., 1968, Borax solution at Kramer, California: Economic Geology, v. 63, no. 8, p. 877-883, https://doi.org/10.2113/gsecongeo.63.8.877.","productDescription":"7 p.","startPage":"877","endPage":"883","costCenters":[],"links":[{"id":373139,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Kramer","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.78099060058595,\n 34.9805024453652\n ],\n [\n -117.50289916992188,\n 34.9805024453652\n ],\n [\n -117.50289916992188,\n 35.110360104213015\n ],\n [\n -117.78099060058595,\n 35.110360104213015\n ],\n [\n -117.78099060058595,\n 34.9805024453652\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"63","issue":"8","noUsgsAuthors":false,"publicationDate":"1968-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Smith, Ward C.","contributorId":42972,"corporation":false,"usgs":true,"family":"Smith","given":"Ward","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":784559,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207280,"text":"70207280 - 1968 - On the maintenance of anomalous fluid pressures: I. thick sedimentary sequences","interactions":[],"lastModifiedDate":"2019-12-15T16:12:30","indexId":"70207280","displayToPublicDate":"1968-12-31T16:07:40","publicationYear":"1968","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":"On the maintenance of anomalous fluid pressures: I. thick sedimentary sequences","docAbstract":"Various physical and chemical processes may be envisioned which will cause anomalous pressures on an underground fluid. In order to consider the maintenance of anomalous pressure, it is necessary to consider the problem as one of nonsteady fluid flow. The time rate of pressure change and maintenance depends upon the hydrodynamics of flow through porous media and the particular boundary conditions. This paper presents a series of general solutions to hydrodynamic models which are germane to the problem of creating and maintaining excess-fluid pressures in a thick sedimentary sequence. The creation and maintenance of fluid pressures approaching lithostatic pressure through a process of continuous sedimentation was evaluated. Our results indicate that a sedimentation rate of 500 m/106 yr (reasonable for the Gulf Coast) will create fluid pressures approaching lithostatic in a sedimentary column that has a hydraulic conductivity of 10-8 cm sec-1, or lower. It is apparent that the creation of anomalous pressure and its maintenance depends, to a large degree, upon the hydraulic conductivity and, to a lesser extent, upon the specific storage of clay layers within the system. © 1968, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1097:OTMOAF]2.0.CO;2","issn":"00167606","usgsCitation":"Bredehoeft, J., and Hanshaw, B., 1968, On the maintenance of anomalous fluid pressures: I. thick sedimentary sequences: Geological Society of America Bulletin, v. 79, no. 9, p. 1097-1106, https://doi.org/10.1130/0016-7606(1968)79[1097:OTMOAF]2.0.CO;2.","productDescription":"10 p. ","startPage":"1097","endPage":"1106","costCenters":[],"links":[{"id":370287,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"79","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bredehoeft, J.D.","contributorId":12836,"corporation":false,"usgs":true,"family":"Bredehoeft","given":"J.D.","affiliations":[],"preferred":false,"id":777528,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":777529,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207279,"text":"70207279 - 1968 - On the maintenance of anomalous fluid pressures: II. Source layer at depth","interactions":[],"lastModifiedDate":"2019-12-15T16:06:21","indexId":"70207279","displayToPublicDate":"1968-12-31T16:00:33","publicationYear":"1968","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":"On the maintenance of anomalous fluid pressures: II. Source layer at depth","docAbstract":"Physico-chemical mechanisms have been suggested to account for anomalous fluid pressures in the geologic environment which require a fluid source at depth. The persistence of anomalous pressure is a problem that involves nonsteady fluid flow. The hydrodynamics and particular boundary conditions control the time rate of pressure change and its maintenance. A series of mathematical solutions germane to the maintenance of anomalous pressure caused by the injection of fluids into the system from a source layer are presented. The phase change, gypsum to anhydrite plus water, is used as an example of a fluid source at depth. The thermodynamics of the gypsum-dehydration reaction indicates that conversion will probably occur at shallow depths and produce fluid at a constant rate. The dehydration of montmorillonite will also produce fluids at a constant rate under geologic conditions where the reaction can occur. If horizons of material of low permeability are missing or scarce, it is doubtful that anomalous pore pressures can be maintained for more than a geologic instant. The creation and continuation of anomalous pressure depend largely upon the hydraulic conductivity and, to a lesser extent, upon the specific storage of clay layers within the system. © 1968, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1107:OTMOAF]2.0.CO;2","issn":"00167606","usgsCitation":"Hanshaw, B., and Bredehoeft, J., 1968, On the maintenance of anomalous fluid pressures: II. Source layer at depth: Geological Society of America Bulletin, v. 79, no. 9, p. 1107-1122, https://doi.org/10.1130/0016-7606(1968)79[1107:OTMOAF]2.0.CO;2.","productDescription":"16 p. ","startPage":"1107","endPage":"1122","costCenters":[],"links":[{"id":370286,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"79","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":777526,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bredehoeft, J.D.","contributorId":12836,"corporation":false,"usgs":true,"family":"Bredehoeft","given":"J.D.","affiliations":[],"preferred":false,"id":777527,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70207397,"text":"70207397 - 1968 - The age of the Puerto Rico Trench","interactions":[],"lastModifiedDate":"2019-12-19T14:04:13","indexId":"70207397","displayToPublicDate":"1968-12-31T15:08:58","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"The age of the Puerto Rico Trench","docAbstract":"The Puerto Rico Trench is parallel to and north of Puerto Rico and the Virgin Islands and reaches depths of more than 8000 meters. Puerto Rico, the closest land area, has a central longitudinal core of Cretaceous and early Tertiary volcanic rocks, some serpentinite of undetermined age, and numerous small intrusions. These rocks were folded into an anticlinorium and intensely faulted into hundreds of fault blocks in an orogeny that lasted from Late Cretaceous until middle Eocene time. Most fold axes and the major fault zones trend approximately west-northwest at an angle of about 15° to the general trend of the island and to the Puerto Rico Trench. Near the north coast, late Oligocene rocks rest on a truncated surface of Cretaceous and early Tertiary volcanic rocks. The Oligocene and overlying Miocene sedimentary rocks strike approximately east, parallel to the Puerto Rico Trench. Apparently the trench is not related to the tectonic movements that folded and faulted the Cretaceous and early Tertiary rocks, but it is closely related tectonically to the Oligocene and Miocene rocks. The trench probably first appeared in Oligocene or possibly late Eocene time and may have reached its maximum depth in late Miocene or Pliocene time.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[487:TAOTPR]2.0.CO;2","issn":"00167606","usgsCitation":"Monroe, W.H., 1968, The age of the Puerto Rico Trench: Geological Society of America Bulletin, v. 79, no. 4, p. 487-494, https://doi.org/10.1130/0016-7606(1968)79[487:TAOTPR]2.0.CO;2.","productDescription":"8 p. 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Some of this displacement occurs as fault slip and some as a more pervasive large-scale drag (oroflexural bending).
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1407:SOREFR]2.0.CO;2","usgsCitation":"Stewart, J.H., Albers, J.P., and Poole, F.G., 1968, Summary of regional evidence for right-lateral displacement in the western Great Basin: GSA Bulletin, v. 79, no. 10, p. 1407-1414, https://doi.org/10.1130/0016-7606(1968)79[1407:SOREFR]2.0.CO;2.","productDescription":"8 p.","startPage":"1407","endPage":"1414","costCenters":[],"links":[{"id":373321,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Great Basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.63037109375,\n 35.92019610057511\n ],\n [\n -115.14221191406249,\n 35.92019610057511\n ],\n [\n -115.14221191406249,\n 38.543869175876154\n ],\n [\n -118.63037109375,\n 38.543869175876154\n ],\n [\n -118.63037109375,\n 35.92019610057511\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"79","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Stewart, J. H.","contributorId":36421,"corporation":false,"usgs":true,"family":"Stewart","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":784994,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Albers, J. P.","contributorId":81505,"corporation":false,"usgs":true,"family":"Albers","given":"J.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":784995,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Poole, F. G. 0000-0001-8487-0799","orcid":"https://orcid.org/0000-0001-8487-0799","contributorId":104883,"corporation":false,"usgs":true,"family":"Poole","given":"F.","email":"","middleInitial":"G.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":784996,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70209121,"text":"70209121 - 1968 - Biostratigraphic classification of the marine Triassic in North America","interactions":[],"lastModifiedDate":"2022-11-22T17:00:10.304171","indexId":"70209121","displayToPublicDate":"1968-12-31T12:23:00","publicationYear":"1968","noYear":false,"publicationType":{"id":4,"text":"Book"},"publicationSubtype":{"id":15,"text":"Monograph"},"title":"Biostratigraphic classification of the marine Triassic in North America","docAbstract":"Ammonoid faunas representative of every major part of Triassic time occur at one place or another in the marine Triassic strata of western and arctic North America. Though some intracontinental provincialism is evident, particularly among Lower and Middle Triassic ammonoid faunas, various local sections where parts of the faunal sequence are preserved—sections in southeastern Idaho, western Nevada, northern California, northeastern Oregon, northeastern British Columbia, southwestern British Columbia, southeastern and southern Alaska, and the Arctic Islands of Canada—can be pieced together in overlapping fashion into a unified sequential framework of biostratigraphic units presented in an annotated zonal chart. At least 35 zonal units of demonstrably different age are now recognized; these units are apportioned among the Griesbachian, Dienerian, Smithian, and Spathian Stages of the Lower Triassic; the Anisian and Ladinian Stages of the Middle Triassic; and the Karnian, Norian and Rhaetian Stages of the Upper Triassic. This zonation based on North American ammonoid faunas for the first time provides an objective and reasonably detailed standard of reference for expressing the age and correlation of the marine Triassic rocks of Canada and the United States.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/SPE110-p1","usgsCitation":"Silberling, N., and Tozer, E.T., 1968, Biostratigraphic classification of the marine Triassic in North America, v. 110, 56 p., https://doi.org/10.1130/SPE110-p1.","productDescription":"56 p.","startPage":"1","endPage":"56","costCenters":[],"links":[{"id":373319,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada, United States","state":"Alaska, Arctic, British Columbia, California, Idaho, Nevada, Oregon","county":"Shasta County","otherGeospatial":"Axel Heiberg Island, Bear Lake area, Ellesmere Island, Keku Straight, Tyaughton Creek, Vancouver Island, Wallowa Mountains, Wrangell Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.640625,\n 76.51681887717322\n ],\n [\n -74.44335937499999,\n 78.50807526258876\n ],\n [\n -63.6328125,\n 81.65968514918798\n ],\n [\n -60.20507812499999,\n 82.4256290002969\n ],\n [\n -64.86328125,\n 83.06877413473718\n ],\n [\n -79.27734374999999,\n 83.23642648170203\n ],\n [\n -95.97656249999999,\n 81.26838476405415\n ],\n [\n -97.3828125,\n 79.9665895843264\n ],\n [\n -92.63671875,\n 78.00732483005181\n ],\n [\n -88.9453125,\n 77.59884823753002\n ],\n [\n -89.47265625,\n 77.0394184427303\n ],\n [\n -89.56054687499999,\n 76.47577254009317\n ],\n [\n -84.375,\n 75.88809074612949\n ],\n [\n -76.640625,\n 76.51681887717322\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -144.404296875,\n 60.59775635343141\n ],\n [\n -142.44873046875,\n 60.59775635343141\n ],\n [\n -142.44873046875,\n 61.51221638411366\n ],\n [\n -144.404296875,\n 61.51221638411366\n ],\n [\n -144.404296875,\n 60.59775635343141\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -133.9796447753906,\n 56.33937887967572\n ],\n [\n -133.6260223388672,\n 56.33937887967572\n ],\n [\n -133.6260223388672,\n 56.610908593846574\n ],\n [\n -133.9796447753906,\n 56.610908593846574\n ],\n [\n -133.9796447753906,\n 56.33937887967572\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.8408203125,\n 42.01665183556825\n ],\n [\n -111.0882568359375,\n 42.01665183556825\n ],\n [\n -111.0882568359375,\n 42.63799988907408\n ],\n [\n -111.8408203125,\n 42.63799988907408\n ],\n [\n -111.8408203125,\n 42.01665183556825\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.17968749999999,\n 38.048091067457236\n ],\n [\n -117.97119140625,\n 38.048091067457236\n ],\n [\n -117.97119140625,\n 40.51379915504413\n ],\n [\n -119.17968749999999,\n 40.51379915504413\n ],\n [\n -119.17968749999999,\n 38.048091067457236\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.44223022460938,\n 44.682324539764934\n ],\n [\n -117.82699584960939,\n 44.682324539764934\n ],\n [\n -117.82699584960939,\n 45.008505958683955\n ],\n [\n -118.44223022460938,\n 45.008505958683955\n ],\n [\n -118.44223022460938,\n 44.682324539764934\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.33526611328125,\n 40.0360265298117\n ],\n [\n -121.35772705078125,\n 40.0360265298117\n ],\n [\n -121.35772705078125,\n 41.2674850985213\n ],\n [\n -123.33526611328125,\n 41.2674850985213\n ],\n [\n -123.33526611328125,\n 40.0360265298117\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.0908203125,\n 48.25394114463431\n ],\n [\n -124.0576171875,\n 49.66762782262194\n ],\n [\n -126.60644531250001,\n 50.680797145321655\n ],\n [\n -127.83691406249999,\n 51.069016659603896\n ],\n [\n -128.8916015625,\n 50.56928286558243\n ],\n [\n -125.24414062499999,\n 48.66194284607006\n ],\n [\n -123.0908203125,\n 48.25394114463431\n ]\n ]\n ]\n }\n },\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -123.05374145507812,\n 50.999928855859636\n ],\n [\n -122.68638610839842,\n 50.999928855859636\n ],\n [\n -122.68638610839842,\n 51.14317120049778\n ],\n [\n -123.05374145507812,\n 51.14317120049778\n ],\n [\n -123.05374145507812,\n 50.999928855859636\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"110","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Silberling, N. J.","contributorId":34919,"corporation":false,"usgs":true,"family":"Silberling","given":"N. J.","affiliations":[],"preferred":false,"id":784991,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tozer, E. T.","contributorId":223413,"corporation":false,"usgs":false,"family":"Tozer","given":"E.","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":784992,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70209119,"text":"70209119 - 1968 - Cenozoic volcanism and sedimentation, silver peak region, western Nevada and adjacent California","interactions":[],"lastModifiedDate":"2020-03-17T12:19:37","indexId":"70209119","displayToPublicDate":"1968-12-31T11:49:07","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Cenozoic volcanism and sedimentation, silver peak region, western Nevada and adjacent California","docAbstract":"Cenozoic deposits of the Silver Peak region, western Nevada, and adjacent California consist principally of continental sedimentary and pyroclastic rocks of the Esmeralda Formation and lavas and tuffs of the Silver Peak volcanic center.
The sedimentary rocks comprise several thick sequences of tuffaceous volcanic sandstone and siltstone and interbedded air-fall tuff. These rocks were deposited in basins that coincide in a general way with the present valleys. Thick wedges of conglomerate and sandstone occur along the basin margins and reflect source areas.
Most of the sedimentary rocks were deposited under fluctuating fluviatile and lacustrine conditions, but paludal conditions prevailed locally. Abrupt facies changes and numerous local unconformities indicate that deposition was not uniform within a given basin.
The sedimentary rocks range in age from late Miocene to late Pliocene. The oldest reliably dated rocks in the Esmeralda Formation are 13.1 m.y. by K-Ar (Barstovian), and all sedimentary strata are younger than an ash-flow sheet dated at 21.5 m.y. by K-Ar. An air-fall tuff in the upper part of the section has a K-Ar age of 4.3 m.y.
Rocks of the Silver Peak volcanic center, 4.8 to 6.1 m.y. by K-Ar, crop out principally in the central part of the Silver Peak Range. Along the margins of the range, they overlie and interfinger with the various sedimentary sequences. The volcanic rocks are mostly rhyolite and trachyandesite tuffs and flows with subordinate basalts and andesites.
Basin and Range faulting began in late early to middle Miocene time and has continued intermittently to the present, but present topography was largely established by late Pliocene time.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Studies in volcanology","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM116-p577","usgsCitation":"Robinson, P.T., McKee, E.H., and Moiola, R.J., 1968, Cenozoic volcanism and sedimentation, silver peak region, western Nevada and adjacent California: GSA Bulletin, v. 116, p. 577-611, https://doi.org/10.1130/MEM116-p577.","productDescription":"36 p.","startPage":"577","endPage":"611","costCenters":[],"links":[{"id":373317,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Nevada","otherGeospatial":"Silver Peak region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -118.29116821289061,\n 37.36470000178872\n ],\n [\n -117.41500854492188,\n 37.36470000178872\n ],\n [\n -117.41500854492188,\n 37.9593578107923\n ],\n [\n -118.29116821289061,\n 37.9593578107923\n ],\n [\n -118.29116821289061,\n 37.36470000178872\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Robinson, Paul T.","contributorId":97562,"corporation":false,"usgs":true,"family":"Robinson","given":"Paul","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":784981,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"McKee, Edwin H. mckee@usgs.gov","contributorId":3728,"corporation":false,"usgs":true,"family":"McKee","given":"Edwin","email":"mckee@usgs.gov","middleInitial":"H.","affiliations":[],"preferred":true,"id":784982,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Moiola, Richard J.","contributorId":82793,"corporation":false,"usgs":true,"family":"Moiola","given":"Richard","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":784983,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70209118,"text":"70209118 - 1968 - O18/O16 ratios of coexisting minerals in glaucophane-bearing metamorphic rocks","interactions":[],"lastModifiedDate":"2020-07-16T19:45:09.972784","indexId":"70209118","displayToPublicDate":"1968-12-31T11:33:38","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"displayTitle":"O18/O16 ratios of coexisting minerals in glaucophane-bearing metamorphic rocks","title":"O18/O16 ratios of coexisting minerals in glaucophane-bearing metamorphic rocks","docAbstract":"Oxygen isotope analyses have been obtained for coexisting minerals in several blue-schist-facies metamorphic rocks from California, Oregon, and New Caledonia. Detailed isotopic studies were made on a continuous exposure of schist in Ward Creek, California, previously described by Coleman and Lee (1962). The oxygen isotope fractionations among coexisting minerals in a variety of rock types, including metasediments and metabasalts, are systematic and larger than those measured in pelitic schists metamorphosed at the grade of biotite zone or higher. Therefore, these Ward Creek rocks (termed Type III) must have formed at lower temperatures than have such pelitic schists.
Evidence for significant isotopic equilibration and homogenization is observed in the Ward Creek sequence. Six different metasediments and metavolcanics collected within 25 m of one another show almost identical mineral δ;-values: quartz (15.8 to 16.3), aragonite (13.1 to 13.3), glaucophane (9.8 to 10.0), muscovite (10.9 to 11.3), lawsonite (9.3 to 9.5), and garnet (8.0 to 8.4), given as per mil enrichment in O18 relative to mean ocean water. These rocks seem to have reached equilibrium at about the same temperature in contact with abundant metamorphic pore fluids.
Not all the Ward Creek rocks have completely equilibrated with the postulated metamorphic pore fluids. In particular, the metacherts seem to have been relatively impermeable to the aqueous fluids during metamorphism, as indicated by the large δ-values of quartz in such rocks (17 to 19.2) and by their appreciably higher Fe+3/Fe+2 ratios. Gradients in O18/O16 and Fe+3/Fe+2 have been generally “smoothed out” in the rocks during metamorphism, but the process has gone to completion only locally. Cherts and limestones have apparently been lowered in O18 content by 10 to 15 per mil, and the metabasalts are enriched by 3 to 4 per mil over their unmetamorphosed parent rocks.
Using the calibrated quartz-muscovite and quartz—CaCO3 geothermometers, the measured quartz-muscovite and quartz-aragonite fractionations indicate essentially “concordant” temperatures of formation for the Type III rocks of 270° to 315° C. Inasmuch as aragonite is part of the equilibrium assemblage, these rocks must therefore have been metamorphosed at pressures of at least 6.4 to 7.0 kb. Oxygen isotope fractionations for the mineral pairs aragonite-lawsonite, quartz-muscovite, and quartz-glaucophane progressively decrease from Type II (low-grade) through Type III to Type IV (high-grade tectonic blocks) metabasalts.
The higher-grade blueschists from New Caledonia exhibit quartz-muscovite and quartz-glaucophane fractionations similar to the Type IV metabasalts at Ward Creek, indicating temperatures of formation of 400° to 550° C. Thus, glaucophane-bearing metamorphic rocks apparently form over a temperature range of 200° C to 550° C, encompassing the probable temperature range of the entire greenschist and epidote-amphibolite facies. This suggests that glaucophane schists should be separated into at least two metamorphic facies, a lower-grade, lawsonite-aragonite blueschist facies and a higher-grade, epidote-rutile blueschist facies, both representing higher pressures than are attained during ordinary low-rank and middle-rank regional metamorphism.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1727:OROCMI]2.0.CO;2","usgsCitation":"Taylor, H.P., and Coleman, R.G., 1968, O18/O16 ratios of coexisting minerals in glaucophane-bearing metamorphic rocks: GSA Bulletin, v. 79, no. 12, p. 1727-1756, https://doi.org/10.1130/0016-7606(1968)79[1727:OROCMI]2.0.CO;2.","productDescription":"30 p.","startPage":"1727","endPage":"1756","costCenters":[],"links":[{"id":373316,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, 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\"}}]}","volume":"79","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Taylor, Hugh P. Jr.","contributorId":101028,"corporation":false,"usgs":true,"family":"Taylor","given":"Hugh","suffix":"Jr.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":784979,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Coleman, Robert G.","contributorId":88022,"corporation":false,"usgs":true,"family":"Coleman","given":"Robert","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":784980,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70209117,"text":"70209117 - 1968 - Age of first marine terrace near Santa Cruz, California","interactions":[],"lastModifiedDate":"2020-03-17T11:29:27","indexId":"70209117","displayToPublicDate":"1968-12-31T11:24:07","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Age of first marine terrace near Santa Cruz, California","docAbstract":"Five species of shallow neritic Pleistocene mollusks from a central California marine terrace give these Th230/U238 ages: 88,000; 68,000; 76,000; 16,000; 100,000; 91,000 (from data in Blanchard and others, 1967). With one exception, the ages fall between 68,000 and 100,000 years. This broad grouping of ages, its general agreement with dates from elsewhere, and geologic evidence suggest that the sea was relatively high in central California sometime during this interval.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1203:AOFMTN]2.0.CO;2","usgsCitation":"Bradley, W., and Addicott, W.O., 1968, Age of first marine terrace near Santa Cruz, California: GSA Bulletin, v. 79, no. 9, p. 1203-1210, https://doi.org/10.1130/0016-7606(1968)79[1203:AOFMTN]2.0.CO;2.","productDescription":"8 p.","startPage":"1203","endPage":"1210","costCenters":[],"links":[{"id":373315,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","city":"Santa Cruz","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -121.94068908691405,\n 36.98116358257264\n ],\n [\n -121.9757080078125,\n 36.96086580957587\n ],\n [\n -122.01828002929686,\n 36.9669008480318\n ],\n [\n -122.03544616699217,\n 36.95483029274437\n ],\n [\n -122.07939147949217,\n 36.953732874654285\n ],\n [\n -122.13157653808594,\n 36.97183825093165\n ],\n [\n -122.20024108886719,\n 37.01351910258053\n ],\n [\n -122.30667114257812,\n 37.125286284966805\n ],\n [\n -122.37258911132812,\n 37.10393176520052\n ],\n [\n -122.21328735351562,\n 36.953732874654285\n ],\n [\n -121.95236206054688,\n 36.90433269687187\n ],\n [\n -121.94068908691405,\n 36.98116358257264\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"79","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bradley, W.C.","contributorId":221699,"corporation":false,"usgs":false,"family":"Bradley","given":"W.C.","email":"","affiliations":[],"preferred":false,"id":784977,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Addicott, Warren O.","contributorId":80668,"corporation":false,"usgs":true,"family":"Addicott","given":"Warren","email":"","middleInitial":"O.","affiliations":[],"preferred":false,"id":784978,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70209116,"text":"70209116 - 1968 - Paleomagnetism, potassium-argon ages, and geology of rhyolites and associated rocks of the Valles Caldera, New Mexico","interactions":[],"lastModifiedDate":"2020-03-17T11:22:21","indexId":"70209116","displayToPublicDate":"1968-12-31T11:16:57","publicationYear":"1968","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Paleomagnetism, potassium-argon ages, and geology of rhyolites and associated rocks of the Valles Caldera, New Mexico","docAbstract":"Paleomagnetic and potassium-argon studies support geologic evidence that the lower member of the Bandelier Tuff was deposited 1.4 m.y. ago. The upper member erupted about 1.0 m.y. ago and was followed by caldera collapse which formed the 12- to 14-mile diameter Valles Caldera. Postcaldera activity which resulted in the eruption of rhyolite domes and pyroclastic material, has occurred at about 0.9, 0.7, 0.5, and 0.4 m.y. ago, with later undated eruptions that were estimated at about 0.1 m.y. ago.
These data from the Valles Caldera are the basis for the previously published age revision of the Brunhes-Matuyama geomagnetic polarity epoch boundary from 1.0 to 0.7 m.y. ago, and they were used to define the Jaramillo normal polarity event at about 0.9 m.y. ago (Doell and Dalrymple, 1966).
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Studies in volcanology","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM116-p211","usgsCitation":"Doell, R., Dalrymple, G.B., Smith, R.L., and Bailey, R.A., 1968, Paleomagnetism, potassium-argon ages, and geology of rhyolites and associated rocks of the Valles Caldera, New Mexico, chap. of Studies in volcanology, v. 116, p. 211-248, https://doi.org/10.1130/MEM116-p211.","productDescription":"39 p.","startPage":"211","endPage":"248","costCenters":[],"links":[{"id":373314,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Mexico","otherGeospatial":"Valles Caldera","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -107.04803466796875,\n 35.61711648382185\n ],\n [\n -106.1883544921875,\n 35.61711648382185\n ],\n [\n -106.1883544921875,\n 36.10015727402227\n ],\n [\n -107.04803466796875,\n 36.10015727402227\n ],\n [\n -107.04803466796875,\n 35.61711648382185\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Doell, Richard R.","contributorId":66683,"corporation":false,"usgs":true,"family":"Doell","given":"Richard R.","affiliations":[],"preferred":false,"id":784973,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dalrymple, G. Brent","contributorId":54564,"corporation":false,"usgs":true,"family":"Dalrymple","given":"G.","email":"","middleInitial":"Brent","affiliations":[],"preferred":false,"id":784974,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Smith, Robert L.","contributorId":90803,"corporation":false,"usgs":true,"family":"Smith","given":"Robert","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":784975,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bailey, Roy A.","contributorId":42576,"corporation":false,"usgs":true,"family":"Bailey","given":"Roy","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":784976,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70207429,"text":"70207429 - 1968 - Alteration of sandstone pipes, Laguna, New Mexico: Discussion","interactions":[],"lastModifiedDate":"2019-12-20T07:12:43","indexId":"70207429","displayToPublicDate":"1968-12-31T10:21:36","publicationYear":"1968","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":"Alteration of sandstone pipes, Laguna, New Mexico: Discussion","docAbstract":"No abstract available.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[787:AOSPLN]2.0.CO;2","issn":"00167606","usgsCitation":"Moench, R.H., and Hilpert, L., 1968, Alteration of sandstone pipes, Laguna, New Mexico: Discussion: Geological Society of America Bulletin, v. 79, no. 6, p. 787-790, https://doi.org/10.1130/0016-7606(1968)79[787:AOSPLN]2.0.CO;2.","productDescription":"4 p. 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Mexico\",\"nation\":\"USA \"}}]}","volume":"79","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Moench, R. H.","contributorId":8853,"corporation":false,"usgs":true,"family":"Moench","given":"R.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":777976,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hilpert, L.S.","contributorId":36619,"corporation":false,"usgs":true,"family":"Hilpert","given":"L.S.","affiliations":[],"preferred":false,"id":777977,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70206944,"text":"70206944 - 1968 - Resurgent cauldrons","interactions":[],"lastModifiedDate":"2019-11-30T08:22:55","indexId":"70206944","displayToPublicDate":"1968-12-31T08:18:19","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2711,"text":"Memoir of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Resurgent cauldrons","docAbstract":"Resurgent cauldrons are defined as cauldrons (calderas) in which the cauldron block, following subsidence, has been uplifted, usually in the form of a structural dome. Seven of the best known resurgent cauldrons are: Valles, Toba, Creede, San Juan, Silverton, Lake City, and Timber Mountain. Geologic summaries of these and Long Valley, California, a probable resurgent caldera, are presented. Using the Valles caldera as a model, but augmented by information from other cauldrons, seven stages of volcanic, structural, sedimentary, and plutonic events are recognized in the development of resurgent cauldrons. They are: (I) Regional tumescence and generation of ring fractures; (II) Calderaforming eruptions; (III) Caldera collapse; (IV) Preresurgence volcanism and sedimentation; (V) Resurgent doming; (VI) Major ring-fracture volcanism; (VII) Terminal solfatara and hot-spring activity. These stages define the terminal cycle of resurgent cauldrons, which in the Valles caldera spanned more than 1 million years. The known and inferred occurrence of the seven stages in the eight cauldrons discussed, together with some time control in four cauldrons, indicates that resurgent doming is early in the postcollapse history; hence, it seems part of a pattern and not fortuitous. Doming of the cauldron block by magma pressure is preferred to doming by stock or laccolithic intrusion, although these processes may be subsidiary. Magma rise that produces doming may be explained in several ways, but the principal cause is not known. Nor is it known why some otherwise similar calderas do not have resurgent domes, although size and thickness of the cauldron block and the degree to which it was deformed during caldera collapse may be factors. All known resurgent structures are larger than 8 miles in diameter and are associated with silicic and, presumably, high-viscosity magmas. Genetically, resurgent cauldrons belong to a cauldron group in which subsidence of a central mass takes place along ring fractures and is related to eruption of voluminous ash flows, thereby differing from Kilauean-type calderas. It is proposed that typical Krakatoan-type calderas differ in that collapse is chaotic and ring fractures are not essential to their formation. Krakatoan calderas typically occur in the andesitic volcanoes of island arcs or the eugeosynclinal environment, and their sub-volcanic analogues are not known, whereas resurgent and related Glen Coe-type cauldrons are more common in cratonic or post-orogenic environments as are their sub-volcanic analogues - granitic ring complexes. Granitic ring complexes, such as Lirue, Sande, Ossipee, and Alnsj0, are probably the closest sub-volcanic analogues of resurgent calderas. The source areas of most of the ash-flow sheets of western United States and Mexico are yet to be found. It is suggested that many of them will prove to be resurgent structures. Present evidence suggests that ore deposits are more commonly associated with resurgent cauldrons than with other cauldron types.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM116-p613","issn":"00721069","usgsCitation":"Smith, R., and Bailey, R.A., 1968, Resurgent cauldrons: Memoir of the Geological Society of America, v. 116, p. 613-662, https://doi.org/10.1130/MEM116-p613.","productDescription":"50 p. ","startPage":"613","endPage":"662","costCenters":[],"links":[{"id":369774,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Smith, R.L.","contributorId":47422,"corporation":false,"usgs":true,"family":"Smith","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":776347,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bailey, R. A.","contributorId":119050,"corporation":false,"usgs":true,"family":"Bailey","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":776348,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70198168,"text":"70198168 - 1968 - Shatter cones at Sierra Madera, Texas","interactions":[],"lastModifiedDate":"2018-07-18T11:46:38","indexId":"70198168","displayToPublicDate":"1968-12-31T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Shatter cones at Sierra Madera, Texas","docAbstract":"Shatter cones abound in the central uplift of Sierra Madera and they occur as far as 6.5 kilometers from the center. Apical angles average near 90 degrees. Whole cones and full cones represented by diversely oriented cone segments in any structural block show relatively uniform orientations of axes and a dominant direction of point. The cones predate faulting and folding in the central uplift, and, when beds are restored to horizontal, most cones point inward and upward, a pattern that supports the hypothesis of an impact origin.
","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.162.3850.261","usgsCitation":"Howard, K.A., and Offield, T.W., 1968, Shatter cones at Sierra Madera, Texas: Science, v. 162, no. 3850, p. 261-265, https://doi.org/10.1126/science.162.3850.261.","productDescription":"5 p.","startPage":"261","endPage":"265","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":355777,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Texas","county":"Pecos County","otherGeospatial":"Sierra Madera crater","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -103.326416015625,\n 29.878755346037977\n ],\n [\n -101.25,\n 29.878755346037977\n ],\n [\n -101.25,\n 31.662732913235317\n ],\n [\n -103.326416015625,\n 31.662732913235317\n ],\n [\n -103.326416015625,\n 29.878755346037977\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"162","issue":"3850","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Howard, Keith A. 0000-0002-6462-2947 khoward@usgs.gov","orcid":"https://orcid.org/0000-0002-6462-2947","contributorId":3439,"corporation":false,"usgs":true,"family":"Howard","given":"Keith","email":"khoward@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":740395,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Offield, Terry W.","contributorId":15196,"corporation":false,"usgs":true,"family":"Offield","given":"Terry","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":740396,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70197756,"text":"70197756 - 1968 - Isotopic age of the Nevadan Orogeny and older Plutonic and metamorphic events in the Klamath Mountains, California","interactions":[],"lastModifiedDate":"2018-06-19T16:38:58","indexId":"70197756","displayToPublicDate":"1968-12-31T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Isotopic age of the Nevadan Orogeny and older Plutonic and metamorphic events in the Klamath Mountains, California","docAbstract":"Several metamorphic and plutonic events have been recognized in the Klamath Mountains utilizing potassium-argon and rubidium-strontium mineral and whole-rock ages. The oldest known metamorphic event in the region produced the Abrams Mica Schist and the co-extensive Salmon Hornblende Schist. Strontium evolution diagrams indicate that the age of primary metamorphism of the Abrams Mica Schist is approximately 380 m.y. (Devonian). The Stuart Fork Formation of Davis and Lipman (1962), the schists of Condrey Mountain, and related schists were produced during a Middle and Late Jurassic metamorphic event. Granitic plutonic rocks are divided into four groups that are different in age and somewhat different in chemical characteristics. The oldest pluton, the Pit River stock, has a minimum age of 246 m.y. (Permian) and is grouped with the Castle Crags pluton. The other three plutonic groups are Middle and Late Jurassic and are characterized by the following ranges in isotopic age: 165 to 167 m.y., 145 to 155 m.y., and 127 to 140 m.y. The principal lode gold deposits in the California part of the Klamath Mountains seem to be related to the youngest group of plutons. If the Nevadan orogeny in this area is restricted to a Middle and Late Jurassic deformational, metamorphic, and plutonic event, the orogeny includes the emplacement of plutons of the three younger groups and the metamorphic development of the Stuart Fork Formation, schists of Condrey Mountain, and related schists.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1027:IAOTNO]2.0.CO;2","usgsCitation":"Lanphere, M.A., Irwin, W., and Hotz, P.E., 1968, Isotopic age of the Nevadan Orogeny and older Plutonic and metamorphic events in the Klamath Mountains, California: GSA Bulletin, v. 79, no. 8, p. 1027-1052, https://doi.org/10.1130/0016-7606(1968)79[1027:IAOTNO]2.0.CO;2.","productDescription":"36 p.","startPage":"1027","endPage":"1052","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":355176,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Klamath Mountains","volume":"79","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Lanphere, Marvin A. alder@usgs.gov","contributorId":2696,"corporation":false,"usgs":true,"family":"Lanphere","given":"Marvin","email":"alder@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":738396,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Irwin, William P.","contributorId":12889,"corporation":false,"usgs":true,"family":"Irwin","given":"William P.","affiliations":[],"preferred":false,"id":738397,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hotz, Preston E.","contributorId":37083,"corporation":false,"usgs":true,"family":"Hotz","given":"Preston","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":738398,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70197571,"text":"70197571 - 1968 - Chittenden, California, earthquake of September 14, 1963","interactions":[],"lastModifiedDate":"2018-06-12T11:28:46","indexId":"70197571","displayToPublicDate":"1968-12-31T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5711,"text":"California Division of Mines and Geology Special Report","active":true,"publicationSubtype":{"id":2}},"seriesNumber":"91","title":"Chittenden, California, earthquake of September 14, 1963","docAbstract":"No abstract available.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Short contributions to California geology","largerWorkSubtype":{"id":2,"text":"State or Local Government Series"},"language":"English","publisher":"California Division of Mines and Geology","usgsCitation":"Brabb, E.E., 1968, Chittenden, California, earthquake of September 14, 1963: California Division of Mines and Geology Special Report 91, 11 p.","productDescription":"11 p.","startPage":"45","endPage":"55","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":354939,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Brabb, E. E.","contributorId":43780,"corporation":false,"usgs":true,"family":"Brabb","given":"E.","middleInitial":"E.","affiliations":[],"preferred":false,"id":737712,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70198175,"text":"70198175 - 1968 - Flow direction in triclinic folded rocks","interactions":[],"lastModifiedDate":"2018-07-18T14:27:30","indexId":"70198175","displayToPublicDate":"1968-12-31T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":732,"text":"American Journal of Science","active":true,"publicationSubtype":{"id":10}},"title":"Flow direction in triclinic folded rocks","docAbstract":"No abstract available.
","language":"English","publisher":"American Journal of Science","doi":"10.2475/ajs.266.9.758","usgsCitation":"Howard, K.A., 1968, Flow direction in triclinic folded rocks: American Journal of Science, v. 266, no. 9, p. 758-765, https://doi.org/10.2475/ajs.266.9.758.","productDescription":"8 p.","startPage":"758","endPage":"765","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":480329,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.2475/ajs.266.9.758","text":"Publisher Index Page"},{"id":355800,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Ruby Mountains","volume":"266","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Howard, Keith A. 0000-0002-6462-2947 khoward@usgs.gov","orcid":"https://orcid.org/0000-0002-6462-2947","contributorId":3439,"corporation":false,"usgs":true,"family":"Howard","given":"Keith","email":"khoward@usgs.gov","middleInitial":"A.","affiliations":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"preferred":true,"id":740430,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70207552,"text":"70207552 - 1968 - Mineralogy of sulfides from certain Hawaiian basalts","interactions":[],"lastModifiedDate":"2020-06-04T13:46:31.899091","indexId":"70207552","displayToPublicDate":"1968-12-23T12:34:58","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Mineralogy of sulfides from certain Hawaiian basalts","docAbstract":"Polymineralic sulfide grains, composed principally of Fe sulfide and Fe-Cu sulfide, with magnetite, have been studied mineragraphically and by electron probe, and interpreted in terms of experimental data for the system Fe-Ni-Cu-S. The three main phases are monosulfide solid solution, a Cu-Fe sulfide (solid solution) with composition near cubanite, and Ti-free magnetite. The grains are believed to represent phases unmixed from an immiscible liquid phase in the basalt magma. Compositions of the two main sulfide phases suggest quenching below 700 degrees C. Most of the Ni has been retained in the monosulfide solid solution by rapid quenching.
","language":"English","publisher":"American Geological Institute","doi":"10.2113/gsecongeo.63.6.636","usgsCitation":"Desborough, G.A., Anderson, A.T., and Wright, T., 1968, Mineralogy of sulfides from certain Hawaiian basalts: Economic Geology, v. 63, no. 6, p. 636-644, https://doi.org/10.2113/gsecongeo.63.6.636.","productDescription":"9 p.","startPage":"636","endPage":"644","costCenters":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"links":[{"id":370652,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Hawaii","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -155.56640625,\n 18.521283325496277\n ],\n [\n -154.22607421875,\n 19.766703551716976\n ],\n [\n -156.357421875,\n 21.22794190505815\n ],\n [\n -158.84033203125,\n 22.30942584120019\n ],\n [\n -160.33447265625,\n 22.43134015636061\n ],\n [\n -160.46630859375,\n 21.861498734372567\n ],\n [\n -155.54443359374997,\n 18.437924653474408\n ],\n [\n -155.56640625,\n 18.521283325496277\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"63","issue":"6","noUsgsAuthors":false,"publicationDate":"1968-09-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Desborough, G. A.","contributorId":34527,"corporation":false,"usgs":true,"family":"Desborough","given":"G.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":778443,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Anderson, Alfred T.","contributorId":210019,"corporation":false,"usgs":false,"family":"Anderson","given":"Alfred","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":778444,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Wright, Thomas L. twright@usgs.gov","contributorId":3890,"corporation":false,"usgs":true,"family":"Wright","given":"Thomas L.","email":"twright@usgs.gov","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true}],"preferred":true,"id":778445,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70209027,"text":"70209027 - 1968 - Ancient geomagnetic field intensities—III historic and archeological data: H13X and H14-15 geological data: G22-29","interactions":[],"lastModifiedDate":"2020-03-11T18:19:46","indexId":"70209027","displayToPublicDate":"1968-12-01T18:15:51","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1804,"text":"Geophysical Journal of the Royal Astronomical Society","active":true,"publicationSubtype":{"id":10}},"title":"Ancient geomagnetic field intensities—III historic and archeological data: H13X and H14-15 geological data: G22-29","docAbstract":"This catalogue contains all ancient geomagnetic field intensity data known to the author at 1968 June 1 and not previously appearing in these lists (Smith 1967c, d). In addition, a short list of publications relevant to the study of ancient field intensities, but containing no new data, is included.
","language":"English","publisher":"Oxford Academic","doi":"10.1111/j.1365-246X.1968.tb02308.x","usgsCitation":"Smith, P., 1968, Ancient geomagnetic field intensities—III historic and archeological data: H13X and H14-15 geological data: G22-29: Geophysical Journal of the Royal Astronomical Society, v. 16, no. 5, p. 457-460, https://doi.org/10.1111/j.1365-246X.1968.tb02308.x.","productDescription":"4 p.","startPage":"457","endPage":"460","costCenters":[],"links":[{"id":480330,"rank":0,"type":{"id":40,"text":"Open Access Publisher Index Page"},"url":"https://doi.org/10.1111/j.1365-246x.1968.tb02308.x","text":"Publisher Index Page"},{"id":373148,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"16","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Smith, P.J.","contributorId":6579,"corporation":false,"usgs":true,"family":"Smith","given":"P.J.","email":"","affiliations":[],"preferred":false,"id":784576,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221382,"text":"70221382 - 1968 - Aquilapollenites: Fossil pollen as seen under the scanning electron microscope","interactions":[],"lastModifiedDate":"2021-06-11T18:44:10.107781","indexId":"70221382","displayToPublicDate":"1968-12-01T13:35:56","publicationYear":"1968","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":"Aquilapollenites: Fossil pollen as seen under the scanning electron microscope","docAbstract":"Photographs of a Late Cretaceous species of Aquilapollenites illustrate the usefulness of the scanning electron microscope (SEM) for the study of fossil pollen. The SEM has the advantages of great depth of focus and wide range of magnification; using present techniques, its use for the study of unsectioned specimens is limited to the observation of surface detail.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1829:AFPASU]2.0.CO;2","usgsCitation":"Drew, C., and Tschudy, B.D., 1968, Aquilapollenites: Fossil pollen as seen under the scanning electron microscope: Geological Society of America Bulletin, v. 79, no. 12, p. 1829-1832, https://doi.org/10.1130/0016-7606(1968)79[1829:AFPASU]2.0.CO;2.","productDescription":"4 p.","startPage":"1829","endPage":"1832","costCenters":[],"links":[{"id":386445,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"79","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Drew, C.M.","contributorId":53089,"corporation":false,"usgs":true,"family":"Drew","given":"C.M.","email":"","affiliations":[],"preferred":false,"id":817461,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tschudy, Bernadine D.","contributorId":74746,"corporation":false,"usgs":true,"family":"Tschudy","given":"Bernadine","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":817462,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221376,"text":"70221376 - 1968 - Salt deposits of the paradox basin, southeast Utah and southwest Colorado","interactions":[],"lastModifiedDate":"2021-06-11T17:21:26.347202","indexId":"70221376","displayToPublicDate":"1968-12-01T12:17:18","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3459,"text":"Special Paper of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Salt deposits of the paradox basin, southeast Utah and southwest Colorado","docAbstract":"Thick salt deposits are present in the Middle Pennsylvanian Paradox Member of the Hermosa Formation in the Paradox Basin of southeast Utah and southwest Colorado. Data suggest that the original thickness of these deposits was from 5000-6000 feet. Locally, however, these deposits have been subjected to intense deformation and flow, resulting in thicknesses as great as 14,000 feet. Each salt bed is part of a series of partial and complete evaporite cycles which show a lateral and vertical change in facies. Varve counts in the salt beds give an indication of deposition rates of time-equivalent carbonate beds. Black sapropelic shales are interbedded with the salt beds. It appears that the euxinic environment in which the shales were deposited persisted during the deposition of salt. An understanding of the stratigraphy of the salt deposits has made possible a more complete depiction of early tectonic events involving the salt basin. These studies indicate that many of the salt anticlines in the basin were formed along trends of originally thick salt beds, and that upward growth of these anticlines possibly began during the late stages of salt deposition.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/SPE88-p319","usgsCitation":"Hite, R.J., 1968, Salt deposits of the paradox basin, southeast Utah and southwest Colorado: Special Paper of the Geological Society of America, v. 88, https://doi.org/10.1130/SPE88-p319.","productDescription":"12 p.","startPage":"320","costCenters":[],"links":[{"id":386439,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Utah, Colorado","otherGeospatial":"southeast Utah, southwest Colorado","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.4013671875,\n 37.055177106660814\n ],\n [\n -107.09472656249999,\n 37.055177106660814\n ],\n [\n -107.09472656249999,\n 38.75408327579141\n ],\n [\n -111.4013671875,\n 38.75408327579141\n ],\n [\n -111.4013671875,\n 37.055177106660814\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"88","edition":"319","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Hite, R. J.","contributorId":82701,"corporation":false,"usgs":true,"family":"Hite","given":"R.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":817452,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70233751,"text":"70233751 - 1968 - A method for estimating the uncertainty of seismic velocities measured by refraction techniques","interactions":[],"lastModifiedDate":"2022-07-27T17:14:44.377534","indexId":"70233751","displayToPublicDate":"1968-12-01T12:02:26","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1135,"text":"Bulletin of the Seismological Society of America","onlineIssn":"1943-3573","printIssn":"0037-1106","active":true,"publicationSubtype":{"id":10}},"title":"A method for estimating the uncertainty of seismic velocities measured by refraction techniques","docAbstract":"Time residuals from 75-km segments of 18 crustal seismic-refraction profiles in the Basin and Range province are used to investigate the validity of the linear-regression model and to make large sample estimates of the variance in the travel time distributions.
A formula for unbiased estimates of velocity uncertainty is derived, assuming a linear trend with distance for the variances of the travel-time distributions. If the recording units are symmetric about the center of the recording interval, this formula is equivalent to the one derived assuming the variances are equal.
At the 95-per cent confidence level the chi-squared test implied 84 per cent of the time-residual samples were inconsistent with the hypothesis that their parent populations had Gaussian distributions. If the number of recording locations expceeds 8, confidence limits computed without the Gaussian assumption suggest the departures from normality are not significant for velocity uncertainty estimates.
The large sample estimates of the time-residual populations may be applicable to other areas. This evidence motivated the development of a method, requiring very little numerical calculation, for estimating uncertainties in velocities. The method requires, in addition to the large sample estimates of the travel time variances, information on the quality of the data, the location of the recording interval, and the number of recording units. The method is useful for the design of new experiments and independent estimates of uncertainty reported in the literature.
","language":"English","publisher":"Seismological Society of America","doi":"10.1785/BSSA0580061769","usgsCitation":"Borcherdt, R.D., and Healy, J.H., 1968, A method for estimating the uncertainty of seismic velocities measured by refraction techniques: Bulletin of the Seismological Society of America, v. 58, no. 6, p. 1769-1790, https://doi.org/10.1785/BSSA0580061769.","productDescription":"22 p.","startPage":"1769","endPage":"1790","costCenters":[{"id":234,"text":"Earthquake Hazards Program","active":true,"usgs":true}],"links":[{"id":404500,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona, California, Idaho, Nevada, Oregon, Utah","otherGeospatial":"Basin and Range province","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.57568359374999,\n 32.45415593941475\n ],\n [\n -111.20361328125,\n 32.713355353177555\n ],\n [\n -111.07177734375,\n 44.29240108529005\n ],\n [\n -123.33251953125,\n 43.6599240747891\n ],\n [\n -123.28857421875,\n 37.70120736474139\n ],\n [\n -121.46484375,\n 34.32529192442733\n ],\n [\n -118.67431640625,\n 32.41706632846282\n ],\n [\n -117.57568359374999,\n 32.45415593941475\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"58","issue":"6","noUsgsAuthors":false,"publicationDate":"1968-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Borcherdt, Roger D. 0000-0002-8668-0849 borcherdt@usgs.gov","orcid":"https://orcid.org/0000-0002-8668-0849","contributorId":2373,"corporation":false,"usgs":true,"family":"Borcherdt","given":"Roger","email":"borcherdt@usgs.gov","middleInitial":"D.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":847627,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Healy, J. H.","contributorId":48968,"corporation":false,"usgs":true,"family":"Healy","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":847628,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221363,"text":"70221363 - 1968 - Palaeomagnetism of a stratiform intrusion in the Pensacola Mountains, Antarctica","interactions":[],"lastModifiedDate":"2021-06-11T14:24:07.996549","indexId":"70221363","displayToPublicDate":"1968-12-01T09:17:32","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2840,"text":"Nature","active":true,"publicationSubtype":{"id":10}},"title":"Palaeomagnetism of a stratiform intrusion in the Pensacola Mountains, Antarctica","docAbstract":"A LARGE stratiform mass of pyroxene gabbro interlayered with smaller amounts of anorthosite and pyroxenite and capped with granophyre makes up most of the northern ranges of the Pensacola Mountains (Fig. 1)1. These layered rocks are at least 2,000 m thick in both the Dufek Massif and the Forrestal Range, and are believed to belong to a single sheet-like body with an areal extent of at least 8,000 km2. The age of the body is not known with certainty, but it intrudes folded rocks as young as Permian (personal communication from J. M. Schopf) and therefore is probably Mesozoic or younger.
","language":"English","publisher":"Wiley","doi":"10.1038/217534a0","usgsCitation":"Beck, M.E., Ford, A., and Boyd, W., 1968, Palaeomagnetism of a stratiform intrusion in the Pensacola Mountains, Antarctica: Nature, v. 217, p. 534-535, https://doi.org/10.1038/217534a0.","productDescription":"2 p.","startPage":"534","endPage":"535","costCenters":[],"links":[{"id":386426,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Antarctica","volume":"217","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Beck, Myrl E. Jr.","contributorId":60700,"corporation":false,"usgs":true,"family":"Beck","given":"Myrl","suffix":"Jr.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":817428,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ford, Arthur B.","contributorId":52578,"corporation":false,"usgs":true,"family":"Ford","given":"Arthur B.","affiliations":[],"preferred":false,"id":817429,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Boyd, W.W. Jr.","contributorId":103359,"corporation":false,"usgs":true,"family":"Boyd","given":"W.W.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":817430,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ]}